Western Michigan University ScholarWorks at WMU
Master's Theses Graduate College
8-1977
Analysis of an Interlobate Boundary in the Wisconsinan Drift of Kalamazoo County and Adjacent Areas in Southwestern Michigan
Norman A. Lovan
Follow this and additional works at: https://scholarworks.wmich.edu/masters_theses
Part of the Geology Commons
Recommended Citation Lovan, Norman A., "Analysis of an Interlobate Boundary in the Wisconsinan Drift of Kalamazoo County and Adjacent Areas in Southwestern Michigan" (1977). Master's Theses. 2207. https://scholarworks.wmich.edu/masters_theses/2207
This Masters Thesis-Open Access is brought to you for free and open access by the Graduate College at ScholarWorks at WMU. It has been accepted for inclusion in Master's Theses by an authorized administrator of ScholarWorks at WMU. For more information, please contact [email protected]. ANALYSIS OF AN INTERLOBATE BOUNDARY IN THE WISCONSINAN DRIFT OF KALAMAZOO COUNTY AND ADJACENT AREAS IN SOUTHWESTERN MICHIGAN
by
Norman A. Lovan
A Thesis Submitted to the Faculty of The Graduate College in partial fulfillment of the Degree of Master of Science
Western Michigan University Kalamazoo, Michigan August 19 77
Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. ANALYSIS OF AN INTERLOBATE BOUNDARY IN THE WISCONSINAN DRIFT OF KALAMAZOO COUNTY AND ADJACENT AREAS IN SOUTHWESTERN MICHIGAN
Norman A. Lovan, M.S.
Western Michigan University, 1977
ABSTRACT
A detailed investigation of selected textural and
mineralogical aspects of tills in southwestern Michigan is
used to define an interlobate boundary relationship be
tween the Wisconsinan ice of the Lake Michigan and Saginaw
lobes. Bedrock underlying the study area contributed lit
tle to the bulk composition of the tills investigated.
However, morainal development in the study area shows
strong correlation with bedrock topography.
In a discussion of the deglaciation of Michigan and
the study area, a history of morainal development is re
viewed and attention is focused on the reentrant district
located in Kalamazoo and neighboring counties. Attempts
to delineate t i l l s of the Lake Michigan and Saginaw lobes
using textural and magnetic susceptibility data were in
conclusive. However, the character and extent of an in
terlobate boundary relationship in the study area is de
limited by ratios of heavy minerals, as well as, ratios of
the 7A/10A peaks produced by clays in X-ray diffractograms.
i i
Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. ACKNOWLEDGEMENTS
I wish to extend my sincere thanks to Dr. W. Thomas
Straw who suggested this problem and encouragingly direct
ed my efforts during the course of the study. My thanks
also go to Drs. Lloyd Schmaltz, W. David Kuenzi, and Cas
par Cronk for their suggestions and review of the manu
script. Appreciation need also be expressed to Dr. W. B. Harrison of Western Michigan U niversity's Geology Depart
ment for suggestions and aid during sample preparation and
to Dr. Stoline of W.M.U.’s Mathematics Department for aid
in the statistical analysis of my data. Additionally, I extend my appreciation to my fellow graduate students, es
pecially Robert Kell, Hall Taylor, Jonathan "Nate” Fuller,
and Warren P. French for th e ir continuous moral support
and criticism and to Bob Havira of Western Michigan Uni
v e rs ity 's Geology Department for photographic work.
To Indiana University, Bloomington, Indiana, and Dr.
J. Mead I express my thanks for the use of their magnetic
susceptibility bridge. Also, to Dr. Ned Bleuer of the
Indiana Geological Survey I extend my appreciation for
suggestions on sample analysis and aid while at Indiana
University. During the first two years of my study I was the re
cipient of Graduate Fellowships funded by Western Michigan
University's Graduate College and the Department of Geo- i i i
Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. i v
logy. Additionally, I received a research grant funded by
the Graduate College.
Finally, I wish to express my gratitude to Linda
Lovan for her continued encouragement, to my parents,
Paul and Mary Lou Lovan, a special appreciation for the
financial and moral aid in what seemed like a c r is is , and
to Janell B. Smith for her assistance in the typing and
preparation of the manuscript, as well as, her personal
friendship. To all these people and many others I extend
my thanks.
*"*' Norman A. Lovan
Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. INFORMATION TO USERS
This material was produced from a microfilm copy of the original document. While the most advanced technological means to photograph and reproduce this document have been used, the quality is heavily dependent upon the quality of the original submitted.
The following explanation of techniques is provided to help you understand markings or patterns which may appear on this reproduction.
1.The sign or "target" for pages apparently lacking from the document photographed is "Missing Page(s)". If it was possible to obtain the missing page{s) or section, they are spliced into the film along with adjacent pages. This may have necessitated cutting thru an image and duplicating adjacent pages to insure you complete continuity.
2. When an image on the film is obliterated with a large round black mark, it is an indication that the photographer suspected that the copy may have moved during exposure and thus cause a blurred image. You will find ja good image of the page in the adjacent frame.
3. When a map, drawing or chart, etc., was part of the material being photographed the photographer followed a definite method in "sectioning" the material. It is customary to begin photoing at the upper left hand corner of a large sheet and to continue photoing from (eft to right in equal sections with a small overlap. If necessary, sectioning is continued again — beginning below the first row and continuing on until complete.
4. The majority of users indicate that the textual content is of greatest value, however, a somewhat higher quality reproduction could be made from "photographs" if essential to the understanding of the dissertation. Silver prints of "photographs" may be ordered at additional charge by writing the Order Department, giving the catalog number, title, author and specific pages you wish reproduced.
5. PLEASE NOTE: Some pages may have indistinct print. Filmed as received.
University Microfilms International 300 North Zeeb Road Ann Arbor, Michigan 48106 USA St. John's Road, Tyler's Green High Wycombe, Bucks, England HP10 8HR
Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. MASTERS THESIS 13^10,287 LOVAN, Norman Alan ANALYSIS OF AN INTERLOBATE BOUNDARY IN THE WISCONSINAN DRIFT OF KALAMAZOO COUNTY AND ADJACENT AREAS IN SOUTHWESTERN MICHIGAN.
Western Michigan University, M.S., 1977 Geology
Xerox University Microfiims,Ann Arbor, Michigan 48106
Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. TABLE OF CONTENTS
PAGE
A b s t r a c t ...... i i Acknowledgements ...... i i i
Table of contents ...... v
List of figures ...... v ii
L ist of t a b l e s ...... x
Introduction ...... 1
Bedrock geology ...... 4
Glacial geology ...... 6
Introduction ...... 6
Till classification ...... 12
Deglaciation of Michigan ...... 17
Terminal and lateral moraines in the study area . 22
Valparaiso morainic system ...... 22
Kendall moraine ...... 24
Kalamazoo morainic system ...... 27
Tekonsha-morainic system ...... 29
L o c a tio n ...... 30
T ech n iq u es ...... 31
Field sampling ...... 31
Laboratory analysis ...... 32 Analysis of an interlobate boundary ...... 35 Textural analysis ...... 37
v
Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. PAGE
Magnetic susceptibility analysis ...... 45
Heavy mineral analysis ...... 52
X-ray diffraction of clays ...... 58
Relationship of bedrock topography to mineral content in local tills ...... 64
Relationship of bedrock topography to morainal development ...... 66
Deglaciation of the study area ...... 72
Summary and conclusions ...... 77 Suggestions for future research ...... 80
References cited ...... 82
Appendix I ...... 89
Appendix I I ...... 117
Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. LIST OF FIGURES
PAGE
Figure I. Map of southwestern Michigan showing the study area and sampling grid, and the maximum eastward extension of the Lake Michigan lobe during Wisconsinan glaciation according to Shah (1971) . . 3
2. Bedrock geology of southwestern Michi gan illu s tr a tin g the study area and the sample g r i d ...... 5 3. Subdivisions of Pleistocene in North America ...... 7 4. Nebraskan, Kansan, Illin o ia n , and Wisconsinan drift borders in North America ...... 9
5. Stratigraphic classification of the Wisconsinan glacial deposits in I l l i n o i s ...... 11
6. Classification of tills showing the relationship between glacial drift in transport to the type of till d e v elo p ed ...... 15
7. Map illustrating Wisconsinan morainal development of the Lake Michigan, Saginaw, and Lake Erie lobes in southern Michigan, and northern Illinois, Indiana, andOhio ...... 18
8. Wisconsinan morainal systems in M i c h i g a n ...... 21 9. Map of southwestern Michigan showing Wisconsinan morainal systems in re lation to Shah’s interlobate boundary (19 71) and the studyare a ...... 2 3 10. Map of southwestern Michigan and the study area showing the location of sample sta tio n s ...... 25
v ii
Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. v i i i
PAGE
Figure 11. Plot of percent sand versus percent mud for samples from deposits of the Lake Michigan and Saginaw lobes .... 39
12. Histogram of the sand/mud ratio of samples from the Lake Michigan and Saginaw lobes showing the mean sand/mud ratio for each group of s a m p le s ...... 40
13. Ternary plot of the very coarse-coarse (18+35 mesh), medium (60 mesh), and fine-very fine (120+230 mesh) sand fractio ns in samples from both the Lake Michigan and Saginaw lobes showing the mean from each group of samples . . 41
14. Graph of percent heavy minerals in the fine plus very fine (120+230 mesh) sand fractio ns in samples from Lake Michigan and Saginaw lobe deposits illu s tra tin g the mean percentage from each group of s a m p le s ...... 42 15. Histogram of the percent heavy minerals in the fine plus very fine (120+230 mesh) sands in samples from deposits of the Lake Michigan and Saginaw lobes illustrating the mean percentage for each group of samples ...... 43
16. Histogram of the magnetic susceptibility of samples taken from deposits of the Lake Michigan and Saginaw lobes i l l u s trating the mean magnetic susceptibi lity of each group of samples ...... 50
17. Ternary plots of heavy mineral assem blages occurring in the fine plus very fine (120+230 mesh) sand fra c tions of samples from t i l l s of the Saginaw and Lake Michigan lobes .... 53
18. Map of the study area showing morainal development, and in terlo b ate boundaries based on garnet/epidote+hornblende ratios, X-ray diffraction analysis of 7A/10A peak- height ratios, and the morphology of weak morainal ridges developed by the Lake Michigan lo b e ...... 56
Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. i x
PAGE
Figure 19. Histogram of garnet/epidote+hornblende ratios from till samples of the Lake Michigan and Saginaw lobes i l l u s t r a ting the mean garnet/epidote+horn blende ratio for each group of sam ples ...... 57
20. X-ray diffractogram s of surface t i l l samples from the Lake Michigan and Saginaw lobes showing the 7A/10A peaks produced by clay minerals .... 59
21. Histogram of 7A/10A peak-height ratios from X-ray diffractogram s of samples from Lake Michigan and Saginaw lobe deposits showing the mean 7A/10A peak-height ratio in each group of s a m p le s ...... 63 22. Map of ice flow directions during the Wisconsinan glaciation of North America showing the provenance and possible movement directions of the jasper conglomerate erratic asso ciated primarily with Saginaw lobe t i l l s ...... 67
23. Map showing the bedrock topography of southwestern Michigan ...... 70
24. Map illustrating the relationship of bedrock topography to morainal deve lopment in southwestern Michigan . . . 71
25. Surface geology of southwestern Michigan. 74
26. Photograph of a fold occurring in the d r if t of the Kalamazoo moraine of the Lake Michigan lobe indicating the overriding and deformation of the moraine by Lake Michigan lobe ice in Wisconsinan t im e ...... 75
Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. LIST OF TABLES
PAGE
TABLE 1. Location, textural, magnetic suscepti bility, X-ray, and garnet/epidote + hornblende d a ta ...... 90
2. Sieve d a ta ...... 99
3. Textural data ...... 105
4. Percent range of predominant heavy m i n e r a l s ...... 51
5. Sample statio n s associated with each half lobe designation ...... 120
6. S ta tis tic a l data from sand/mud ra tio , percent heavy minerals in the fine + very fine (120+230 mesh) sands, mag netic susceptibility, X-ray diffrac tion, and garnet/epidote+hornblende ratio analyses ...... 121
7. Mann-Whitney U Test for sand/mud ratio and percent heavy minerals in the 120+230 mesh s a n d s ...... 124
8. Mann-Whitney U Test for magnetic su s c e p tib ility and X-ray d iffra c tio n d a t a ...... 125
9. Mann-Whitney U Test for garnet/epidote + hornblende d a ta ...... 126
1 0 . T Test for sand/mud ratio and percent heavy minerals in the 120+230 mesh s a n d s ...... 127
11. T Test for magnetic susceptibility and X-ray diffraction d a ta ...... 128 12. T Test for garnet/epidote+hornblende d a t a ...... 129
x
Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. INTRODUCTION
Development of the surface geology of southwestern
Michigan occurred during the Wisconsinan glaciation of
North America. Of particular interest to this study are
the g la c ia l deposits in Kalamazoo County and the adjacent
areas produced by the interplay of the Lake Michigan and
Saginaw lobes of the Wisconsinan ice. To date, no relia
ble statistical data have been used to delineate the limits
of these deposits; however, a complete understanding of
the glacial history of Michigan necessitates some compre
hension of the boundary relationships between them.
Chamberlin (1883a and 1883b) introduced the term
"interlobate moraine" for features "formed by the joint action of two glaciers (or glacial lobes) pushing their
marginal moraines together" to produce a common boundary. Realizing the complex regional nature of the interplay of
glaciers in an interlobate area, a more general definition
would be of greater value. Thus, as defined by Rieck
(1976) and used herein, an interlobate area is an area of
drift accumulation developed in or near the reentrant dis
trict between two lobes of glacial ice. Moraines develop
ed in such an area may have formed when active glacial
moraines were in contact or when the active glacial ice
margins had retreated and exposed a narrow zone, 1 mile
1
Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. (1.6 km) to several miles, between them (Rieck, 19 76).
Using the above d e fin itio n , much of southwestern
Michigan, and in p a rtic u la r Kalamazoo County, is a classic
interlobate area (Leverett and Taylor, 1915; Wayne and
Zumberge, 1965; Farrand and Eschman, 1974). Shah (1971) defined and drew an interlobate boundary depicting the
eastern most extension of the Lake Michigan lobe in south
western Michigan (Fig. 1) based on the morphology of weak
morainal ridges that parallel known deposits of the Lake
Michigan lobe.
The present study is an effort to statistically de
fine and establish the interlobate boundary relationship
produced by the in terp lay of the Lake Michigan and Saginaw
lobes in areas in and adjacent to Kalamazoo County, Michi
gan, by determining the provenance of glacial tills.
Rieck (1976) delineated t i l l s of the Saginaw and Huron-
Erie lobes in southeastern Michigan utilizing X-ray dif
fraction techniques, and Bleuer (1975) distinguished tills
in Indiana derived from different source areas by esta
blishing ratios of various heavy minerals. Studies in
surrounding regions have also been successful in esta
blishing till provenance by using mineralogic and other
techniques (Gravenor, et a l . , 1976; Derry, 1934; Anderson,
1957; Gravenor, 1951). In the present study, textural and
mineralogic data are utilized to describe the character,
extent, and contact relationship of the tills left by the
Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 1 NORTH r EATON CO ------CALHOUN CO “I BRANCH CO S/< s BARRY BARRY CO I — I ALLEGAN CO CASS CO ST JOSEPH CO VAN VAN BUREN CO | | 1 —J BERRIEN CO Interlobate Boundary Sample grid S tu d y are a EXPLANATION m iles Figure .1. Map of southwestern Michigan showing the study area and sampling grid, and and the eastward maximum extension of the Lake Michigan lobe during Wisconsinan g laciatio n according to Shah (1971) «
Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Lake Michigan and Saginaw g lac ia l lobes. Not only is an
understanding of the nature of deglaciation in southwes
tern Michigan enhanced, but also relatively new techniques
proven successful in other regions are used and tested in
establishing the interlobate boundary in the study area.
BEDROCK GEOLOGY
The bedrock geology of Michigan consists of two dis
tin c t provinces (Wayne and Zumberge, 1965). All of the
Southern Peninsula and the eastern h a lf of the Upper (Nor
thern) Peninsula consists of Cambrian to Pennsylvanian
shales, sandstones, carbonates, and evaporites of the
Michigan Basin. The western half of the Upper Peninsula
of Michigan exposes rocks of the Precambrian Canadian
Shield. These rocks are mainly Early Precambrian, Keewatin
through Algoman, g ran ites, greenstones (metamorphosed lava
flows), and metasediments; Middle Precambrian, Animikian,
iron formations and in tru siv e s; and Late Precambrian, Ke-
weenawan, lava flows, conglomerates, and sandstones (Wayne
and Zumberge, 1965; Dorr and Eschman, 19 71).
Unconsolidated glacial sediments of the study area
are underlain by the Lower Mississippian Coldwater Shale
and Marshall Sandstone (Fig. 2). No known bedrock out
crops appear in the study area. The present knowledge of
bedrock characteristics within the study area is based on
well logs from Kalamazoo County and bedrock outcrops in
Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Cn EATON COALLEGAN CO EATON COALLEGAN BRANCH BRANCH CO BARRY BARRY CO i i r t ST ST JOSEPH CO . . KALAMAZOO CO Me 1 VAN VAN BUREN CO DERR EN DERR . . Miss. ]■ Penn. Penn. Study area U. Sample grid Saginaw & Parma 3. Miss. &/or Dev. Mid. Dev. Ellsworth Ellsworth-Antrim Traverse Explanation Coldwater
T | m miles [ E rr—I u. Dev I Pu i El r°"»i | | Mm | Michigan |Mnm| Napoleon & L. Marshall r ~ I Pflr I 7 1 Grand River H | Mbp | Bayport t t % Figure 2. Bedrock geology of southwestern Michigan (after the Michigan Geologi (g rey ). cal Survey, 1968) illustrating the study area (heavy line) and the sample grid
Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 6
adjacent areas (Shah, 1971).
As reported by Shah (1971), the Coldwater Shale in
southwestern Michigan is dominantly blue to grey and grades
upward into the Lower Marshall Sandstone. Trending north
westward across Kalamazoo County, the Coldwater Shale forms
a belt approximately 25 miles (40 km) in width beneath the
surface drift material (Shah, 1971). Within the shales
are thin discontinuous zones of limestone, dolomite, and
clay ironstone concretions.
The Lower Marshall Sandstone occupies portions of the
northeast corner of the study area (Fig. 2). Winchell
(1861) described the Lower Marshall Sandstone as being
white, grey, green, and red in color. Clay ironstone con
cretions are present in sandy shale lenses which are local
ly micaceous. Plant impressions and pockets of coal have
also been reported (Shah, 1971). Paralleling the Coldwater
Shale within the study area, the Marshall Sandstone strikes
northwest and dips gently northeastward toward the basin's
center.
GLACIAL GEOLOGY
Introduction
The Pleistocene Epoch was marked by several world
wide, synchronous glaciations. In North America at least
four separate periods of continental glaciation have been
Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 7
recorded (Fig. 3).
The Nebraskan glaciation extended as far south as
Kansas and Missouri (Fig.4). Buried beneath younger drift
wherever it occurs, Nebraskan drift is best developed in
northern Missouri, eastern Nebraska, and northeastern Kan sas (Flint, 1957). At the close of the Nebraskan glacia
tion a period of clim atic warming occurred and has been
named the Aftonian Interglacial (Chamberlin, 1895).* Dur
ing the Aftonian and before subsequent glacial advance,
grasses and trees flourished as recorded in the pollen of
so il p ro file s and peat lenses lying between Nebraskan and
Kansan d r if t sheets (F lin t, 1957).
Glacials Interglacials Y.B.P.
0 Recent Wisconsinan 10,000 Sangomonian Illin o ian Yarmouthian Kansan Aftonian Nebraskan 1.5 Million
Figure 3. Subdivisions of the Pleistocene in North America (a fte r Dorr and Eschman, 1971).
*Interglacials are periods of clim atic warming be tween periods of glacial advance or glacials.
Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 8
West of the Mississippi River Kansan Age drift extends
beyond younger drift sheets but is overlapped by Illinoian
drift in Illinois, Indiana, and Ohio. Two lobes of Kansan
ice are shown in Illinois (Fig. 4); however, Flint (1957)
stated that the existence of two Kansan lobes in Illin o is
is questionable considering the "scanty" subsurface data
available. The Yarmouthian Interglacial separating the
Kansan and Illin o ian glacials is represented by a so il zone
developed in Kansan d r if t. Simonson (1954) compared so ils
developed in Kansan d r ift with modern equivalents and s t a
ted that the Yarmouthian climate was much like that of the
present.
Illinoian drift is best developed in Illinois with its overall drift border following a similar outline as the
subsequent Wisconsinan glaciation (Fig. 4). Tills of Illi
noian Age are reported as being rich in clay and silt.
Leverett and Taylor (1915) described a t i l l in southeastern
Michigan which they attributed to Illinoian glaciation.
Evidence for multiple periods of glacial advance dur
ing Illin o ian time e x ists. Frye and Leonard (1954) e sta
blished that a soil zone developed within the Illinoian
sediments of Kansas implies a period of warm climate that
endured for several thousand years. Studies in Nebraska
and Missouri yield correlative results (Thorp, et al. 1951;
and Davis, unpublished data in Flint, 1957). The Illinoian and Wisconsinan glaciations are separa-
Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. ID NEBRASKAN WISCONSINAN KANSAN ILLINOIAN 1*1. EXPLANATION Jjl*1 r*5 — * — r*5 (WIS 200 MINN MILES Figure 4. Nebraskan, Kansan, Illinoian, and Wisconsinan drift borders in North Am e rica (modified from F lin t, 1957).
Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 10
ted by a period of warmer climate called the Sangamon
Interglacial. Sangamon soils are well developed and show
about the same regional changes as do modern so ils (F lin t,
1957; Flint, 1971).
Perhaps the best known and differentiated period of paleoglaciation is that of the Wisconsinan Age. This is
easily understood when it is realized that Wisconsinan
glaciation ended less than 10,000 years ago. At its maxi
mum extent, Wisconsinan ice reached into southern Ohio,
Indiana, and Illinois. From Illinois, the Wisconsinan
border extends westward and north through Iowa, Nebraska, and the Dakotas, then on to the Rocky Mountains (Fig. 4).
The stratigraphy of the Wisconsinan deposits are
better known than that of any other glacial age. Since around 1950, a detailed reexamination of Wisconsinan Age
deposits has been undertaken and their classification re
viewed. Leighton (1960) and Willman and Frye (1970) e s
poused classifications of Wisconsinan stratigraphy which
are in use today. However, the c la s s ific a tio n of Leighton
(1960) appears to be preferred by researchers studying
Michigan's glacial deposits.
Practically all of the surface deposits covering
Michigan's lower peninsula are glacial in origin. The
majority of these deposits are the result of ice advance
and re tre a t phases of the Cary, Port Huron (Mankato), and Valders substages of the Wisconsinan glaciation (Fig. 5).
Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 1 1 R a d i o MODIFIED AFTER MODIFIED AFTER c a r b o n LEIGHTON, 1960 FRYE AND WILLMAN, y .b .p . 1970 0
5,000 HOLOCENE RECENT 10,000 * VALDERAN STAGE TraTn'P'Dc: bct ijn s mC ln T it Twocreek Int. TWOCREEKAN MANKATO (PORT L a t e STAGE HURON) GLACIAL > Bowmanvilie / w / u I n t . f 15.000 < CARY GLACIAL St. Charles 3 WOODFORDIAN < I n t . 3 STAGE H TAZAWELL GLACIAL CD CO 3 G a r d e n a I n t. t O 20.000 IOWAN GLACIAL •H U INAN ICONS AGE CQ & H H 25,000 3 F a rm C r e e k 3 FARMDALIAN Interglacial STAGE j 30.000 ■ 35.000 FARMDALE GLACIAL ALTONIAN ------STAGE E a r ly *7^/D/UUU nnn ----- SANGAMON AGE SANGAMONIAN AGE
Figure 5. Stratigraphie classification of the Wiscon sinan glacial deposits in Illinois (modified from Shah, 1971) .
Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 12
Very few, if any, exposures of pre-Wisconsinan tills occur
at the surface in Michigan. Thus, only the glacial his
tory of Michigan during Wisconsinan time, more precisely
from Cary time to the Recent, is discussed.
Till Classification
Prior to the evolution of the glacial theory in the
second quarter of the 19th century, erratic boulders were
recognized as being deposits of transported materials
(Charlesworth, 1957; Flint, 1971). Originally these de
posits were believed to have been lowered to the earth’s
surface after floating on ice across the landscape dur
ing the great Biblical deluge. Subsequently, Sir Charles
Lyell, in 1830, espoused the "Drift Theory" to explain
the d istrib u tio n of these e rra tic s and Murchison (1836)
recommended the term d r if t be used in order to avoid fu r
th er relig io u s connotations. With time, and the develop
ment of the idea that glaciers once occuppied regions far
more extensive than at present, the term "Glacial Drift" has evolved to embrace all rock material in transport by
glacial ice, all deposits made by glacial ice, and all
deposits largely of glacial origin (Flint, 1971).
Drift has subsequently been subdivided into three
basic categories based primarily on the sedimentological
characteristics: stratified drift, unstratified drift,
and erratic boulders and clasts. Stratified drift (out-
Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. wash) is that m aterial deposited in d irectly from the ice
by the action of glacial meltwaters. As outwash and er
ratic boulders are not topics of discussion in this paper,
no further attempt will be made to define or classify them
But, because this study deals with unstratified drift
(till) the definition and classification of such material
is included.
Till, a Scottish word used to describe a coarse ob
durate land, is defined as an aggregate whose components
are brought together and deposited directly by glacier ice
(Boulton, 1972). Being more variable than any other sedi
ment, till is a mixture of grain sizes and rock types
(Goldthwait, 1971; Flint, 1957). Any given grain size may
constitute the bulk of an accumulated till, and the rock
types are dependent on the geologic formations over which
the glacier has ridden.
Tills have been variously classified by origin, color
texture, degree of compaction, lithologic composition, and
mode of deposition (Dreimanis, 1971). Perhaps the most
useful and fundamental classification is based on genesis;
however, the most distinctive and easily recognized pro
perties of tills are those acquired during the process of
deposition. Thus, the most satisfactory classification is
one based on depositional modes (Flint, 1957; Boulton,
1972) .
Using the above d efin itio n and u tiliz in g the subgla-
Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. cial, englacial, and supraglacial criterion of glacial
debris in transport (Fig* 6), t i l l s may be c la ss ifie d in the following manner:
A. Lodgement or basal till, deposited subglacially from d r ift m transport in the base of an active glacier. The de b ris is released from the ice by slow pressure melting of the flowing ice and lodged in the accumulating drift on the subglacial floor (Chamberlin, 1894; Dreimanis, 1967a; Flint, 1957; Boulton, 1972). The resulting till lacks sort ing, is compact, and often acquires a fissile structure (Flint, 1971).
B. Ablation till, deposited from en- glacial and supraglacial debris in the terminal area of a glacier. The glacial material is lowered to the ground as the ice melts inward from the term inus, top, and base (F lin t, 1957). T ills produced by this method are characteristically loose, noncompact, and n o n fissile .
Following several years of research with modern arctic g laciers as depositional models, Boulton (1972) suggested
th a t, by using the above c la s s ific a tio n , existin g models
for the interpretation of ancient tills and the sequences
in which they lie are often too simple. Going even further
Boulton stated that "many Pleistocene and earlier sequences
currently thought of as products of repeated glacier ad
vance and readvance, may be products of a single retreat phase by a glacier with a thick englacial debris load."
With th is in mind Boulton offers a refinement of the
ablation till category as follows:
A. Flow till, released supraglacially
Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. M cn
(by (by lodgement or basal melting ) (by means(by of surface melting) Basal till Ablation till Dreimanis, 1967a
Basal or Flint, 1957 Local till Ablation till Lodgement till Deformation till Flow till Boulton, 1972 Melt-out till
drift drift Englacial Subglacial in transport
rock rock or Sediment Glacial Drift Glacial Figure 6. Classification of tills showing the relationship between glacial drift in o Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 16 and undergoing subsequent deformation as a result of subaerial flow (Boulton, 1972) . T ills developed by th is method, are very often brought from a subgla cial position to a supraglacial posi tion along debris bands within the ice and therefore may contain many features characteristic of basal tills (Boulton, 1968). B. Melt-out tills, deposited either supraglacially or subglacially from stagnant ice beneath a confining over burden (Boulton, 1970b; Boulton, 1972). In a glacial sequence from which the ice has vanished, melt-out tills re present the stratigraphic position of the depositing glacier (Boulton, 1970). The significance in Boulton's refinement (1972) is that the ablation till/basal till doublet postulated by F lin t (1957) may develop e n tire ly suprag lacially . As sub glacial till is brought to a supraglacial position along glacial debris bands, subsequent downslope flow may trans late parts of the till to the upper surface of the ice. Once exposed to subaerial processes, sorting of the upper portion of the till may produce a lower massive element with an upper, washed and often crudely stratified element. If then, given the association of supraglacial outwash, tripartite till/outw ash/till sequences may develop which are the result of a single glacial retreat phase rather than multiple advance and retreat (Boulton, 1968; 1971; 1972).* *For information on fabric data as related to tills, see Holmes, 1941, Flint, 1957, 1971, and Boulton, 1971. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Deglaciation of Michigan The glaciation of Michigan during Cary time was ac complished by the nearly simultaneous advance of glacial ice via the Lake Michigan, Lake Erie, and Saginaw basins (Wayne and Zumberge, 1965). Completely covering Michigan, the Cary ice extended into southern I llin o is , Indiana, and Ohio. At its maximum extension, 18,000 years ago, the Cary ice stood near the Ohio River and resulted in the deposition of the Minooka, Iroquois-Packerton, and Union City term inal moraines (Fig. 7) of the Lake Michigan lobe, Saginaw lobe, and Erie lobe respectively (Eschman and Farrand, 1974). As the ice of all three glacial lobes began to retreat from its position of maximum extension, the Saginaw lobe ice dissipated more rapidly than the ice of the Lake Michi gan and Lake Erie lobes. Leverett (1915) reasoned th a t, during advance, the Saginaw lobe ice had overridden an area of greater topographic relief than either the Lake Michigan or Lake Erie lobes. The resulting thickness of Saginaw ice must, therefore, have been less than that of its counter parts and the movement of Saginaw ice correspondingly weaker. Additionally, Leverett (1915) added that excessive loading of Saginaw lobe ice resulting from convergence with the adjacent Lake Michigan and Lake Erie lobes may also have effected the weaker movement of the Saginaw lobe. With con- 17 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 00 NORTH Saginaw lobe drift drum llns m e ltw a te r Explanation Saginaw lobe moraines Erlelobedrlfton TH m ( fogf Erie lobe morainesE 3 L-- J Lake moraines Michigan lobe 11 11 Tazewell moraines MILES MICHIGAN LAKE Figure 7. Map illustrating Wisconsinan morainal development o£ the Lake Michigan, U, U, Union City moraine; Ms, Mississinewa moraine; Sa, Salamonie moraine; Fw, Fort Wayne Ti, TinleyS, moraine; Sturgis V, moraine; Valparaiso T, moraine; Tekonsha moraine; I, Mx, Maxinkuckee Iroquois moraine; moraine; P, K, Packerton Kalamazoo moraine; moraine; Saginaw, and Lake Erie lobes in southern Michigan, and northern I llin o is , Indiana, and moraine; Wa, Wabash moraine; D, Defiance moraine). Ohio (a fte r Zumberge, 1960: W, West Chicago moraine; M, M arseilles moraine; Mi, Minooka moraine; Ma, Manhattan moraine; C, Chatsworth moraine; LB, Lake Border moraine; Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 19 tinued retreat of Cary ice, the first portion of Michigan (south-central Michigan) to become ice free occurred ap proximately 15,000 years b.p. (Wayne and Zumberge, 1965). Evidence for the more rapid retreat of Saginaw lobe ice as compared with ice of the Lake Michigan and Lake Erie lobes is found 2 8 miles (45 km) southwest of Ann Arbor, Michigan, and in Steuben and DeKalb Counties, Indiana. At these locations clay-rich tills of the Erie lobe overlie sandier textured t i l l s of the Saginaw lobe (Zumberge, 1960; Wayne and Thornbury, 1955; Wayne and Zumberge, 1965). Additional support exists in northeastern Indiana and south-central Michigan where outwash sands and gravels of the Erie lobe occupy areas previously inhabited by the Saginaw lobe (Wayne and Zumberge, 1965). The strongest evidence supporting rapid recession of Saginaw ice , as well as providing a means of co rrelation for Cary age moraines, is the Kankakee Torrent. Ekblaw and Athy (1925) established the coalescence of melt-water channels heading at the Tekonsha moraine of the Erie lobe (Fig. 7). The Kankakee Torrent discharged southwestward along the east-southeastern edge of the Lake Michigan lobe and across the northwestern corner of Indiana to Illinois. Dreimanis and Morner (1973) recognized a major flu c tuation in the Erie lobe ice that was synchronous with the to rre n t, the Erie Interstad e. Kunkle (1963) correlated lake beds in southwestern Ontario with erosional channels Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 20 in the Huron River valley which indicates ice recession north of Lake Erie approximately 15,600 years ago. Far- rand and Eschman (1974) noted th a t an o sc illa tio n of th is magnitude has not yet been recognized for the ice of the Lake Michigan lobe. Following the Erie Interstade, the ice readvanced into southeastern Michigan culminating about 14,800 years ago (Dreimanis and Morner, 1973). From this point in time the Cary ice continued its overall retreat with only minor re advances . The Cary ice retreated northward to approximately the Straits of Mackinac. A bryophyte bed is exposed nine miles (14.4 km) south of the s t r a it s in Cheboygan County (Far- rand, et al., 1969). Radiocarbon dates of 13,300 y.b.p. are given for material from this bed. This 1 cm thick mat of mosses indicates that the Cary ice front must have r e trea te d at le a st th is far north (Farrand and Eschman, 1974). Readvance of the ice in Port Huron time resulted in the formation of the Port Huron moraine, 13,000 y.b.p. (Hough, 1958) (Fig. 8). According to Dorr and Eschman (1971), all glacial deposits south of the Port Huron moraine are Cary in age. The Port Huron ice reached as fa r south as Muskegon and Milwaukee (Farrand and Eschman, 1974). Tills of this moraine are characterized as being blue to grey-blue and quite sandy in places (Wayne and Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 21 miles Explanation W isconsinan end moraines 1 Sturgis moraine 2 Tekonsha moraine 3 Kalamazoo moraine 4 Kendall moraine Figure 8. Wisconsinan morainal systems in Michigan (after Michigan Geological Survey, 1975). Zumberge, 1965). In contrast, the later Valderan tills are red to pink. With recession of Port Huron ice, Valders ice advanced from the northeast to a p o sitio n proximal to the Port Huron Moraine in the northern part of the Southern Peninsula (Wayne and Zumberge, 1965). No end moraines were built by Valderan ice, but drumlins near Grand Traverse Bay trend northwestward indicating a radial flow from the central Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 22 Lake Superior region (Wayne and Zumberge, 1965). With re treat of the last Valderan ice, all of Michigan was ice free about 10,000 years b.p. (Broecker and Farrand, 1963) leaving behind the present glacial landforms (Fig. 8). Terminal and Lateral Moraines in the Study Area The study area, which centers in Kalamazoo County, was completely covered by two lobes of the Wisconsinan con tinental glacier. The Lake Michigan lobe advanced into the study area from the northwest. The Saginaw lobe ad vanced from the northeast. With final retreat of the ice fronts in Cary time, bold morainic systems were left to cover the landscape. Portions of five (5) morainal systems in the study area were left by the Lake Michigan and/or Saginaw lobes. The Lake Michigan lobe is responsible for portions or all of the Valparaiso, Kendall, Kalamazoo, Tekonsha, and Sturgis moraines. The Saginaw lobe built portions of the Kalamazoo, Sturgis, and Tekonsha moraines (Fig. 9). The following morainal descriptions are based largely on work by Leverett and Taylor (1915). Valparaiso morainic system A segment of the Valparaiso morainic system of the Lake Michigan lobe occupies the northwestern corner of the Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. study area in southeastern Allegan County and northeastern Van Buren County, Michigan (Fig. 9). This morainic system extends from the Wisconsin-Illinois line around the sou thern end of Lake Michigan through northern Indiana and northward to near Rockford, Michigan. Here it joins its correlative moraine of the Saginaw lobe. The Valparaiso morainic system constitutes the drai nage divide at the head of Lake Michigan separating waters flowing to the St. Lawrence and M ississippi Rivers. Topo- EXPLANATION Wisconsinan end moraine Interlobate boundary (Shah, 1 9 7 1 ) Figure 9. Map of southwestern Michigan showing Wiscon sinan morainal systems in relation to Shah's Interlobate boundary (1971) and the study area (morainal systems a fte r Michigan Geological Survey, 1975; V, Valparaiso; K, Kendall T, Tekonsha; Ka, Kalamazoo; S, S tu rg is). Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 24 graphic relief along the inner border of the moraine is quite conspicuous, rising 100 to 200 feet or more to its crest (Leverett and Taylor, 1915) . Conversely, the relief along the outer border is somewhat less, ranging in general from 50 feet or less to around 75 feet. The thickness of drift averages about 200 feet along the entire extent of the moraine in Indiana and Michigan, but a wide range of till compositions exists over this distance. The Wisconsinan drift in Illinois tends to be a blue clayey till. Eastward toward Valparaiso, Indiana, clay continues to predominate over sand and gravel, but beyond this, to the northeast, sand and gravel are predo minate over clay. Sample stations 58 and 59 (Fig. 10) are located on the Valparaiso moraine. Tills at these locali ties are very sandy with boulders ranging to 8 inches (20.32 cm) in diameter. Most boulders consist of igneous and metamorphic lithologies of Canadian Shield derivation. Kendall moraine The Kendall moraine is located in the northeastern corner of Van Buren County a few miles north of Paw Paw, Michigan (Fig. 9). Approximately nine miles (14.4 km) long in a northeast-southwest direction, the Kendall moraine averages 1.5 to 2.5 miles (2.4 to 4 km) in width. North of the village of Kendall knolls exhibit a re lief of 60 to 80 feet (18.28 to 24.38 m), whereas, south Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 73 CD ■o-5 o Q. C o CD Q. ■o CD (C/)f) O CO BARRY COALLEGAN EATON CO ■Oo Expl anation >74 75 CALHOUN CO 29/32(^14^3 gg 40 3"3. Primary stations CD VAN BUREN CO CD ■o Secondary stations o 38* 42 Q. C a Study area o ■o KALAMAZOO CO o CD Q. miles BERRIEN CO COST. JOSEPH COCASS BRANCH CO ■o CD NORTH C/) C/) Figure 10. Map of southwestern Michigan and the study area (heavily outlined) show ing the location of sample stations. Secondary sample stations are circled. l/ltv) 26 of the village the relief averages 25 to 30 feet (7.62 to 9.14 m). Extending northeastward, the Kendall moraine ter minates in a swamp. East of this swamp a weak ridge ex tends to the northeast and connects with the inner border of the Kalamazoo moraine. Because of this relationship, Leverett (1915) assigned the Kendall moraine to the Kala mazoo morainal system of the Lake Michigan lobe. Dis agreeing with Leverett, Terwilliger (1954) correlated the Kendall moraine with the Valparaiso morainic system. By studying terraces of equal elevation along the sides of the Dowagiac Drainageway and the east side of Prospect Hill, Terwilliger concluded that Prospect Hill and the low moraine upon which Decatur is situated are contemporaneous with the Kendall moraine. Till samples from eight locations were collected along the Kendall moraine (Fig. 10, stations 23 through 29, and 31). Its tills are generally poorly consolidated, sandy to bouldery, and red to red-brown in color. Leverett (1915) reported blue t i l l at depths w ithin the moraine and characterized the surface appearance as being bouldery. Shah (1971) recorded the presence of red jasper conglo merate at the north end of the Kendall moraine. Because the red jasper conglomerate is predominantly associated with Saginaw lobe depo sits, Shah (1971) asserted th a t the Kendall moraine is a deposit of the Saginaw lobe. In a Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 27 paper concerning the source of the above red jasper con glomerate e rr a tic s , Slawson (1925) sta te d the following: MIn the Wisconsin drift the eastern limit of these erratics is marked in Michigan by the moraines bordering the glacial lake beds and in Ohio by a line running south of Norwalk through Mansfield and east of Dayton. On the west a lim ited number of the boulders have been deposited by the eastern half of the Lake Michigan lobe. In general, though, the great bulk of them were transported by the ice of the Saginaw lobe." X-ray data and analysis of heavy minerals on samples col lected on the Kendall moraine show conclusively that tills of the Kendall moraine belong to the Lake Michigan lobe. Kalamazoo morainic system The Kalamazoo morainic system was constructed by the joint action of the Lake Michigan and Saginaw lobes. The junction of the two correlative morainic systems is lo cated slig h tly north of the study area in Barry County (Fig. 9). It is here that the Kalamazoo morainic system reaches its greatest elevation, 1050 feet above sea level. In Michigan the Kalamazoo moraine of the Lake Michigan lobe is comprised of two nearly parallel ridges which trend in a northeast-southwest direction. The outer ridge (eas tern ridge) extends from Prairieville southwestward to South Bend, Indiana, where it is interrupted by a gravel plain along the St. Joseph River. The inner or western ridge parallels the outer ridge and is traceable to a loca- Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 28 tion approximately six miles (9.6 km) west of South Bend. The relief along the outer border is slight as a gravel plain is built up nearly to its crest throughout its length. Conversely, the relief along the inner border ridge ranges from 50 feet (15.2 m) in southern Michigan to 200 feet (60.9 m) as the moraine extends northward. Surface tills of both the inner and outer moraines are loose textured and range from clay-rich to very sandy. Cobbles to 8 inches (20.3 cm) in diameter commonly occur dispersed in the till. In most instances the surface drift is less than 1.5 meters thick and is underlain by strati fied and often crossbedded sands and gravels. A grey or bluish clay-rich compact t i l l is located at sample sta tio n 3 (Fig. 10) at the corner of Ravine Road and Douglas Ave nue in Kalamazoo, Michigan. Similar tills are found ex posed in 30 to 50 foot cliffs in the Lake Border moraine along the Lake Michigan shore line in Allegan County (Fig. 10, stations 60 and 61). Perhaps the blue clay-rich nature is due to the underlying Lower Mississippian Coldwater Shale (Fig. 2). The Kalamazoo morainic system of the Saginaw lobe joins its correlative system of the Lake Michigan lobe in southwestern Barry County (Fig. 9). From this junction the Saginaw lobe portion of these moraines extends southeast ward and eventually connects with the Mississinawa moraine of the Huron-Erie lobe in Washtenaw County. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 29 Relief along the Saginaw lobe portion of the morainic system is slight. In most places it is little more than 30 feet (9.1 m) and rarely exceeds 50 feet (15.2 m). In Jackson County the area around Portage swamp has 150 feet (45.7 m) of relief and is the most prominent portion of the moraine. Tills within the moraine are generally sandy, result ing from erosion of the underlying sandstone units. Boul ders of local bedrock and Canadian Shield derivation are commonly abundant. Tekonsha morainic system *»**"- 4 Within the study area, the Tekonsha morainic system is located in western Calhoun County and eastern Kalamazoo County (Fig. 9). The Tekonsha moraine of the Saginaw lobe is joined at its northwest and southeast ends by correla tive moraines of the Lake Michigan and Huron-Erie lobes, respectively, and has a general width of 4 to 5 miles (6.4 to 8 km). Its counterpart from the Lake Michigan lobe ex tends southwestward from the junction and averages appro ximately 3 miles (4.8 km) in width. The southwestward extension of the Tekonsha moraine of the Lake Michigan lobe is well developed for approxi mately 8 miles (10.8 km). Based on the location and mor phology of the eastern side of the Sturgis moraine of the Lake Michigan lobe, Straw (1977, personal communication) Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 30 is of the opinion that this portion of the Sturgis moraine may have developed synchronously with, and therefore, re present an extension of the Tekonsha moraine. Tills of the Tekonsha moraine are typically sandy and boulder strewn. The sandy nature results in large part from the underlying and neighboring Lower Marshall Sand stone. It should be noted that boulders of the Lake Mich igan lobe’s Sturgis and Tekonsha moraine are lithologically sim ilar. A north trending spur of the Sturgis moraine in Cass and St. Joseph Counties projects into the study area. Sample statio n s 64 and 65 (Fig. 10) indicate that t i l l s of this moraine are sandy textured and lithologically similar to those of the Tekonsha moraine. As only a small portion of the Sturgis moraine is represented in the study area (Fig. 9), a discussion of this morainal system is omitted. LOCATION -The area under in v estig atio n , centering in Kalamazoo County, lies in the southwestern Michigan interlobate re gion of the Central Lowlands physiographic province (Fig. 1). Located on the southwestern flank of the Michigan basin, the entire study area is covered by glacially de rived sediments. Here the glacial materials are charac terized by bold morainal deposits and associated sand and gravel outwash plains. Tills within the area are generally Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 31 loose textured although compact tills are locally distri buted. Ibrahim (1969) reported that the drift thickness in Kalamazoo County ranges from 50 to 650 fee t (15.2 to 198.1 m) and according to Malanchak (1973) the average thickness is between 290 to 390 feet (88.4 to 118.9 m). The midpoint of the study area lies approximately 136 miles (217.6 km) west of Detroit, 50 miles (80 km) south of Grand Rapids, and 112 miles (179.2 km) east of Chicago. TECHNIQUES Field Sampling In order to establish a statistical basis for initial sampling, a grid was designed which traversed the study area in a northwest-southeast direction (Fig. 1). Using the in te rlo b a te boundary mapped by Shah (1971) as a focal point, the grid area was extended into regions of known Lake Michigan and Saginaw lobe deposits, thereby insuring the positioning of the interlobate boundary within the grid. Sample collection was controlled by till outcrop ex posure, and representative till samples were collected by entrenching the exposures. The location of each station is recorded in Table 1 of Appendix I and in Figure 10. Following the laboratory analysis of the initial or Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 32 primary samples, an interlobate boundary was established within the grid. Subsequently, additional or secondary stations were randomly established and representative samples were collected and analyzed in order to define an interlobate boundary throughout the remainder of the study area. Laboratory Analysis Analytical techniques described in this section in clude various methods for obtaining textural, magnetic susceptibility, X-ray, and heavy-mineral data. Results utilizing these techniques are then presented in the sec tion titled "Analysis of an Interlobate Boundary Relation ship ." Using modifications of procedures outlined by Folk (1968), a ll samples were dried at 100°F for a minimum of eight hours. Samples were then tran sferred to the labora tory preparation room where they were disaggregated and allowed to equilibrate with room temperature and humidity. The gravel portion of each sample was removed by passing the entire sample through a 10 mesh (2.00 mm) sieve. Gravel portions of each sample were marked and stored; a split (approximately 200 grams) of the remaining clays, s i l t s , and sands was obtained and washed in 200 ml of calgonated de-ionized water for a minimum of 24 hours. A second s p lit (75 to 100 grams) of the remaining clays, Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 33 silts, and sands was obtained. This representative of the "bulk sample"* was taken to Indiana University (Bloo mington) for analysis of magnetic susceptibility (see section on magnetic susceptibility). Clays and s i l t s were separated from the sand fra c tions by wet sieving using a 63 micron (230 mesh, 0.0625 mm) sieve and de-ionized water. The muds were washed into a 1000 ml graduated cylinder, stirred, and allowed to settle for 24 hours. Subsequently, basally-oriented clay mounts were prepared for X-ray diffraction analysis by pippetting a clay-rich suspension onto glass slides and drying at room temperature. Dried basally-oriented clay mounts were placed in a d essicator p a rtia lly fille d with ethylene glycol for an additional 24 hours. It should be noted th at slides number 3c, 10, 12, 14, 16a, 17, 18, 20, 23, 27, 29, and 31 had to be remade because of sh rin kage during drying. Remaking was accomplished by passing the residual silts and clays through a 325 mesh sieve, mixing with distilled de-ionized water, and preparing clay mounts as described above. The remaining mud/water solution was transferred to 1000 ml beakers, dried, and stored. After wet sieving and removal of the mud fractions *Bulk sample is defined as the split sample exclud ing the gravel fraction and is recorded in Table 1 of Appendix I. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. from the sand fractions of each sample, the cleaned sands were washed into beakers and dried at 125°F. Dried sand samples were then split and weighed. The splits of each sand sample were sieved into very coarse, coarse, medium, fine, and very fine sand fractions (10, 18, 35, 60, 120, and 230 mesh sieves), and each fraction weighed (Table 1 of Appendix I ) . Sands from the 120 and 230 mesh sieves were combined for heavy mineral analysis. Following the procedure outlined by Krumbein and Pettijohn (1938) and modified by Kuenzi (1974), heavy mineral separations in the fine and very fine sand frac tions (120 + 230 mesh) were accomplished using bromoform (CHBrg, d=2.89 at 20°C) and washing with acetone ((CHj^ CO). Each combined 120 plus 230 mesh sample was poured into a separatory funnel fille d with bromoform having a specific gravity of 2.89 at 20°C. The samples were stirred every thirty minutes for three hours, then allowed to set tle for two hours (5 hours total) before the heavy minerals were drawn off. Upon final separation of heavy-mineral concentrations, each sample was air dried, weighed, and split into portions preparatory to mounting on glass slides. Grain mounts were prepared by coating heated petro- graphic slides with a combination of approximately 0.110 grams of heavy minerals per sample and caedex (synthetic Canada balsam ). Upon fin al curing of the caedex, a glass cover slide was applied and grains dispersed by manipula- Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 35 tion of the cover glass. Grinding of the grain mounts was unnecessary as grains ranging from 100 to 200 mesh yield first order colors when illuminated under a polarizing microscope (Bloss, 1961). Using a Lietz polarizing microscope and mechanical stage, a total of 500 garnet versus epidote plus hornblende determinations were counted per slide. Data accumulated using this technique may be found in Table 1 of Appendix I. ANALYSIS OF AN INTERLOBATE BOUNDARY In the past, the history of the deglaciation of any given area has been based primarily on the morphology of bold morainal systems left by the retreating ice mass. Michigan has been no exception. The deglaciation of Michi gan during Wisconsinan time left the state covered with bold morainal systems (Fig. 8). Careful examination of these moraines and other data have resulted in major works by Leverett and Taylor (1915), Hough (1958), and Wayne and Zumberge (1965), as well as many others. Their contribu tions have tremendously added to the knowledge of continen tal deglaciation during the Pleistocene. Recent studies have focused more and more attention on the problem of unraveling the history of areas which developed by the complex in te rac tio n of two or more lobes of ice during the same or repeated glaciation. To do this, many analytical techniques have been developed and tested. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 36 In this study, textural, magnetic susceptibility, X-ray diffraction, and heavy mineral data are used to establish the character of an interlobate boundary in the study area. Textural parameters have been frequently utilized in describing and differentiating glacial sediments. In this study, two techniques based on textural analysis of till matrix (materiaK 2 mm) were used in an attempt to dif ferentiate till (Dreimanis and Vagners, 1972). The per cent sand/percent mud ratio and the percent heavy minerals in the 120 plus 230 mesh sands were calculated. Both parameters were statistically analyzed. The results are presented in following sections. Textural data accumu lated by exercising the above methods of analysis can be found in Tables 1-3 of Appendix I. The use of magnetic susceptibility (MS) as a tool for the differentiation of glacial sediments based on proven ance has been well established in the last decade (Vonder Haar and Johnson, 1973; Gravenor and Stupavsky, 1974; Gravenor, et al., 1976). Utilizing the facilities of Indiana University's Department of Geology (Bloomington), the magnetic susceptibility of samples from the initial grid area were determined and statistical analysis subse quently performed. The results are presented in following sections and the Appendix. It has long been recognized that the composition of a Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 37 till is reflective of the bedrock lithologies over which the glacier traversed. Thus, it follows that if two dis tinct glaciers or glacial lobes originated in similar but different areas, the composition of their resulting tills should be dissimilar, or at the very least, show differ ing ratios between any given suite of minerals. Based on this assumption, heavy mineral analysis was undertaken and a ratio of garnet/epidote plus hornblende calculated for all samples. The data was statistically analyzed and the results are presented in subsequent sections and Appendix I and II. The use of X-ray diffraction techniques to differen tiate glacial drift from differing sources has been in vestigated in a number of studies (Frye, 1968; C a stillio n , 1972). Rieck (1976), working in an interlobate area of southeastern Michigan, was able to differentiate tills of the Saginaw and Huron-Erie lobes by using X-ray diffrac tion of clays. Modifying the methods of Rieck (1976), and Glass (personal communication, 1976) and Gluskoter (1967) o of the Illinois Geological Survey, analysis of the 7A and © 10A clay peaks was undertaken. The results are statisti cally analyzed and presented in succeeding sections and the Appendix. Textural Analysis Tills are more variable than any other sediment (Gold- Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 38 thwait, 1971). Gravels, sands, silts, and clays indi vidually may constitute the bulk of any given till and local variation from one extreme to another is common. Examination of textural data (Table 1 of Appendix I and Fig. 11) shows that the percent of sand in samples col lected from deposits of the Lake Michigan lobe ranges from 25 to 9 7 percent. The percent of mud for the same lobe ranges from 3 to 75 percent. Samples collected from Sagi naw lobe material exhibit some overlap, having a range of 50 to 94 percent sand and 6 to 50 percent mud. It is noteworthy that within the study area Lake Michigan lobe ice eroded bedrock parallel to the strike of the under lying Coldwater Shale and Marshall Sandstone; whereas, Saginaw lobe ice eroded bedrock perpendicular to this strike. Thus, it may be hypothesized that the resulting Lake Michigan lobe tills within the study area may contain a greater proportion of clay than the opposing Saginaw lobe tills. On this assumption, a ratio of percent sand to percent mud (%sand/!mud) was calculated and s t a t i s t i cally analyzed for all surface data (see Appendix II). Comparison of the mean sand/mud ratio for the Lake Michi gan and the Saginaw lobe tills support the above hypo thesis (Fig. 11 and 12). Lake Michigan lobe tills exhibit a mean sand/mud ratio of 2.249 while Saginaw lobe tills show a mean of 4.095 (Fig. 12). The Chi Square Test indi cates that the sand/mud ratio of the sample population Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. without prohibited reproduction Further owner. copyright the of permission with Reproduced PERCENT SAND ecn sn ad 99 pret mud). percent 19.90 and sand percent samples_from deposits of the Lake Michigan and Saginaw Saginaw and Michigan Lake the of deposits samples_from lobes (Xa, mean for Lake Michigan lobe = 69.45 percent sand sand percent 69.45 = lobe Michigan Lake for mean (Xa, lobes and 31.55 percent mud; Xb, mean for Saginaw lobe = 81.10 81.10 = lobe Saginaw for mean Xb, mud; percent 31.55 and 100 0 _ 60 20 _ 70 so 0 _ 50 0 _ 30 Figure 11. Plot of percent sand versus percent mud for for mud percent versus sand percent of Plot 11. Figure _ _ _ 20 30 PERCENT MUD □ Lake Michigan Lake lobe □ Xa Xa lobe Saginaw • Xb Xb 060 40 en ae ihgn lobe Michigan Lake Mean en aia lobe Saginaw Mean 070 50 90 100 39 from each lobe is not normally d istrib u te d (see Appendix I I ) . The Mann-Whitney U Test for independence showed no significant difference in the populations from each lobe (Table 7, Appendix II). Yet, according to the Student T Test (Table 10, Appendix II) the difference in the mean sand/mud ratio for each lobe is significant at the 0.10 level. However, only levels of significance less than or equal to 0.05 are considered geologically significant in this study, although a level of significance of 0.10 clear- 16 - Saginaw lobe 14 - Lake Michigan lobe 12 - > Xa Mean Lake Michigan lobe zo 10 H UJ Xb Mean Saginaw lobe U° 0ft J—! cc Xa 6 - Xb 4 — uanaaaanaanana EL aa aa o D D D E b b b b b 0 —i i i I I I i i i i i H F I. i H i . FI 1 2 ] 3 41 5 6 8 9 10 11 12 13 Xa Xb SAND/MUD RATIO Figure 12. Histogram of the sand/mud ratio of samples from the Lake Michigan and Saginaw lobes showing the mean sand/mud ra tio for each__group of samples (Xa, mean Lake Michigan lobe = 2.249; Xb, mean Saginaw lobe = 4.095). Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. (41 very coarse & coarse sand LAKE MICHIGAN LOBE SAGINAW LOBE X a MEAN LAKE MICHIGAN LOBE Xb MEAN SAGINAW LOBE □ • fine A very fine sand medium sand Figure 13. Ternary p lo t of the very coarse-coarse (18+35 mesh), medium (60 mesh), and fine-very fine (120+230 mesh) sand fractions in samples from both the Lake Michigan and Saginaw lobes showing the mean from each group of samples. ly indicates the general truth of the assumption. A ternary plot of the very coarse-coarse, medium, and fine-very fine sand fractions in samples from both the Lake Michigan and Saginaw lobe deposits illustrates that differ ences in texture of the matrix sand are small and overlap (Fig. 13). Similar overlap is observed when the percent of fine and very fine sand (120 plus 230 mesh) is plotted against the percent of heavy minerals from those fractions Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. (Fig. 14) and in the histogram of percent heavy minerals in the fine plus very fine sand (120 plus 230 mesh) from both lobes (Fig. 15). The Student T Test indicates that the difference in the heavy mineral content of the fine plus very fine sand fraction (120 plus 230 mesh) occurring in samples from both the Lake Michigan and Saginaw lobes Saginaw lobe 80 - (D Lake Michigan lobe O Xa Mean Lake Michigan lobe iuco 2 60 - Xb Mean Saginaw lobe CO©1 CM © o CM 40 - < CO ottl s ttl 20 o. T 10 PERCENT HEAVY MINERALS ^120 + 230 MESH X 100) Figure 14. Graph of percent heavy minerals in the fine plus very fine (120+230 mesh) sand fractio n s in samples from Lake Michigan and Saginaw lobe deposits illu s tr a tin g the mean percentage from each group of samples (T, total sand recalculated to 1001; Xa, mean Lake Michigan lobe = 2.6 70; Xb, mean Saginaw lobe = 3.133). Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 43 is significant at the 0.10 level. Again, however, the re sults are considered inconclusive (see Table 7, Appendix II). Local variation in texture is often observed. For example, statio n s 22a and b, 31a and b, and 32a through d (Fig. 10) show variation in texture within a very local area (Table 1 of Appendix I ) . Samples a and b from sta tio n 14 - Saginaw lobe 12 - Lake Michigan lobe, 10 _ > ’a Mean Lake Michigan lobe.Xa o z 8 _ Xb _ U13 Mean Saginaw lobe ...... Xb a DD iii 6 _ n o e DD a . on DD 4 _ OBI BBOB DBDD DBDD 2 — DODD H BDBBB BHDDD BDBBB ODBBB P l:|:l r l:|:l i FI 1 i tl il 5 6 7 8 Xa Xb PERCENT HEAVY MINERALS IN THE 120+230 MESH SANDS Figure 15. Histogram of the percent heavy minerals in the fine plus very fine (120+230 mesh) sands in samples from deposits of the Lake Michigan and Saginaw lobes i l lustrating the mean percentage for each group of samples (Xa, mean Lake Michigan lobe = 2.670; Xb, mean Saginaw lobe = 3.133). Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 44 22 (Fig. 10) were collected from sites separated by a lateral distance of approximately 30 feet (9.14 m). Sta tion 22a contains 31.25 percent sand and 68.75 percent mud, whereas, 22b contains 60.64 percent sand and 39.36 percent mud. Variation in percent sand and mud taken in a vertical sequence was observed at stations 31 and 32 (Table 1 of Appendix I). Thus, because of variation and overlap in matrix textures both regionally and locally, delineation using textural data is inconclusive. The texture of till is dependent on four factors: lithologic contribution of bedrock, comminution (depen dent on mode of transport, either supraglacial, englacial, or subglacial), possible sorting of rocks and minerals during transport, the process of deposition, and post- depositional change (Dreimanis and Vagners, 1972). How ever, the texture of till matrix (that material less than 2 mm in size) depends mainly on the terminal grades of its constituent minerals (Dreimanis and Vagners, 1972) . A rock or mineral’s terminal grade is the final pro duct of comminution. Particle size range in till depends on the original size of the mineral grains when incor porated within the ice, as well as, their resistance dur ing transport and distance of transport (Dreimanis and Vagners, 1972). Larger grade sizes of most rocks and minerals are reduced to under one-tenth of a percent of Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 45 the original size in 8 to 80 kilometers of transport (Goldthwait, 1971). Most resistant minerals are brought to their terminal grade after 80 to 180 kilometers of glacial comminution (Dreimanis and Vagners, 1972). The terminal grade of garnets and other heavy minerals ranges from 2 to 50 (Dreimanis and Vagners, 19 71). The texture, as well as the composition, of till is greatly influenced by the composition of the local bed rock. However, because the study area is almost completely underlain by the Lower Mississippian Coldwater Shale, the effect of the local bedrock on the texture and composition of till is reduced. Therefore, the similarity and over lapping nature of the till matrix textures for the Lake Michigan and Saginaw lobe deposits within the study area can be attributed to the far traveled character of the till matrix. Magnetic Susceptibility Analysis The magnetic susceptibility (MS) of tills is depen dent on the amount and distribution of the ferromagnetic minerals within the till, as well as, on the strength of the magnetic field employed in its measurement (Nagata, 1961). The property measured is the density magnetic sus ceptibility and represents the ratio of the intensity of magnetization produced in a substance to the magnetizing force to which i t is subjected (Vonder Haar and Johnson, Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 46 1973) . Jones and Beavers (1964a) utilized magnetic suscep tibility measurements to differentiate loess deposits in Illinois. Differences in susceptibility for these depo sits reflected mineralogic differences which were inter preted to reflect differences in provenance. Gravenor and Stupavsky (1974) were able to differentiate tills found south of the Precambrian-Paleozoic boundary in Ontario using magnetic susceptibilities. Magnetic susceptibility measurements were determined for samples from the initial grid area (stations 1 through 57, Fig. 10). Comparison of MS measurements with lobe designations based on X-ray and heavy-mineral analysis (Table 1 of Appendix I) shows no significant difference between the Lake Michigan and Saginaw lobe deposits. Statistical analysis of these data yield similar results (Appendix II). The Chi Square Test indicates that a non normal distribution exists for populations from both the Lake Michigan and Saginaw lobes (Appendix II). The Mann- Whitney U Test and Student T Test both accepted their respective Null Hypothesis which state that two indepen dent samples are from the same population, and the means of each population are equal (see Tables 8 and 11 of Appendix II). The lack of correlation of MS values and till pro venance for samples within the study area cannot be singu Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 47 larly explained. Several possibilities exist which could produce inconclusive data. First, inconclusive data may be obtained if the samples are weathered (Bleuer, 1976, personal communication). Oxidation and leaching of the till may change the valence states of the ferromagnetic minerals, thereby creating a likelihood of obtaining un reliable MS data. However, Gravenor and Stupavsky (1974), in Ontario, made MS measurements on samples from four lo calities in which both oxidized and unoxidized samples were used. The results obtained were identical within their range of accuracy. In a similar study, Vonder Haar and Johnson (1973) found th at oxidized samples collected within their study area yielded essentially the same MS as unoxidized samples from the same location. Nonetheless, they further state that "in other situations or types of material, oxidation may influence the magnetic properties." The question which should be asked is, if the samples are weathered to the point of causing erroneous magnetic susceptibility data, would not the data obtained from clay mineral and heavy mineral analysis also be effected? In a discussion of weathered samples, Krumbein and P e tti- john (1938) concluded th at the e ffe cts of oxidation are on the iron-bearing minerals. They further stated that min- eralogic changes may or may not occur in oxidized samples. Assuming the conclusion of Krumbein and P ettijohn is tru e, samples taken from the study area could be oxidized and Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 48 therefore yield anomalous magnetic susceptibility while simultaneously yielding definitive mineralogic results. With this in mind, it is noteworthy that in this study, ratios of garnet versus epidote plus hornblende are suc cessfully used to establish lobe provenance. Second, as the area under investigation is an inter- lobate zone, the possibility of mixing exists. Oscillating lobes of ice may have mixed the concentrations of ferro magnetic minerals which effect MS. The viability of this explanation is somewhat diminished, however, when it is noted that clay and heavy mineral data are successfully used to delineate deposits of the Lake Michigan and Sagi naw lobes. Presumably, had mixing occurred, not only would the concentrations of ferromagnetic minerals have been mixed, but also the clays and heavy minerals used in establishing g la c ia l lobe provenance would have been mixed as w ell. In considering the above, a question which arises is, Mis it possible that mineralogic mixing could occur such that magnetic susceptibility appears similar in the oppo sing glacial tills, but yet, the clay mineralogy and heavy mineral content of the tills remain distinctive? Straw (1976, personal communication) observed that Saginaw lobe deposits near the airport in Kalamazoo, Michigan, show evidence of having been pushed by ice from the west (Lake Michigan lobe ic e ). Shah (1971) designated several weak Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 49 moraines in Saginaw lobe drift which parallel known depo sits of the Lake Michigan lobe as push moraines. Examination of the mean magnetic susceptibility for deposits of the Lake Michigan and Saginaw lobes may lend support to the above question. The mean MS of the depo sits of the Lake Michigan lobe is 3.218 x 10 ~4 cgs. Simi larly, the Saginaw lobe deposits exhibit a mean value of 3.131 x 10 4 cgs. If, however, the deposits delineated as Lake Michigan lobe and Saginaw lobe material are divided into their respective east and west halves, a mean of 2.875 x 10 ~4 cgs is given for the eastern half of the Lake Michigan lobe and 3.565 x 10 “4 cgs for the western half. From observation of magnetite sands along Lake Michigan's shore such an increase might be expected. The eastern half of the Saginaw lobe deposits shows a mean MS of 3.085 x 10" 4 cgs while the western half exhibits a 3.114 x 10 "4 cgs. The question now a risin g is , "is th is phenomena of the westward increase in mean MS for tills from the Lake Michigan lobe and the eastward decrease in mean MS for the Saginaw lobe t i l l s the re su lt of mixing and i f not, then what?" The final possibility is that there is little or no difference in the values of magnetic susceptibility for samples collected within the study area. Statistical analysis of magnetic susceptibility data tends to substan tiate this possibility. Examination of the histogram (Fig. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 50 16) for MS shows overlap in the frequency of occurrence of MS for samples taken from the Lake Michigan and Saginaw lobes. The graph shows a marked similarity in percent frequency of occurrence. Additional support is found when it is noted that a similar overlap occurs when comparing percentages of ferromagnetic and other heavy minerals 2 0 “ I 18 - Saginaw lobe 16 - Lake Michigan lobe 14 - Xb Xa Xa Mean Lake Michigan lobe O> 12-1 z UJ Xb Mean Saginaw lobe o 10 - 111 lla 8 - 6 - 4 - 2 - I Fl ■ FFF -ii :m |:n i 6 i 7 4 Xb MAGNETIC SUSCEPTIBILITY r. 10~4 CGS Figure 16. Histogram of the magnetic susceptibility of samples taken from deposits of the Lake Michigan and Sagi naw lobes illustrating the mean magnetic susceptibility of each group of samples (Xa, mean Lake Michigan lobe = 3.218; Xb, mean Saginaw lobe = 3.131). Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. (Table 4). Gravenor and Stupavsky (1974) established that there is a sig n ific a n t co rrelatio n between the amount of mag n etic m aterial and the amount of heavy minerals in a t i l l Till samples taken from the study area show a range of 0.69 to 6.85 percent weight of heavy minerals for Lake Michigan lobe tills and 1.42 to 7.66 percent weight of heavy minerals for Saginaw lobe tills. Therefore, a lack of correlation of magnetic susceptibility and provenance for tills within the study area may be due to the similar ity, as well as, the variability of the percent range of heavy minerals. However, as a majority of the samples collected are from oxidized surface exposures, the effect of weathering cannot be discounted. TABLE 4. Percent range of predominant heavy minerals. Minerals observed but not included in Table are rutile, apatite, staurolite, and kyanite. Range of percent occurrence Mineral Lake Michigan lobe Saginaw lobe Hornblende 50-631 37-57% Magnetite 14-241 7-28% B io tite 4- 9% 4-14% Epidote 1-10% 6 - 22% Garnet 0-11% 11-16% Tourmaline 0 - 1% 0- 1% Sphene 0- 31 0- 7% Zircon 0 - 1% 0- 1% Pyrite 0 - 2% 0- 1% Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Heavy Mineral Analysis The study of heavy minerals in glacial tills is well established in the geologic literature (Derry, 1934; Drei manis and Reavely, 1953; Dreimanis, et al., 195 7; Breene, 1957; Brophy, 1959; Frye, Williams, and Glass, 1960; S it- ler, 1963). Gravenor (1951), in a study of heavy mineral suites from southwestern Ontario tills, concluded that the heavy minerals were contributed mainly by the crystalline rocks of the Canadian Shield. Similar observations were made by e a r lie r workers (Krumbein, 1933; Kruger, 1937) in establishing the provenance of tills. By assuming that heavy mineral suites in tills are reflective of provenance, it follows that ratios of heavy minerals can be statistically used to distinguish tills from separate glaciers. To test this assumption 15 ran domly chosen thin-section grain mounts containing heavy minerals from the fine and very fine sand fractions were selected from samples of each lobe. Three hundred grain determinations were made per slide. Ternary plots of heavy mineral data obtained from this analysis illustrate the viability of delineating tills based on provenance by this method (Fig. 17). Bleuer (1975) had success in delineating tills of the Lake Michigan, Saginaw, and Erie lobes in Indiana by such a method. He reports that the Lake Michigan lobe tills are 52 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 53 Sphene Magnetite • Saginaw lobe □ Lake Michigan lobe Garnet Epidote Hornblende Figure 17. Ternary plots of heavy mineral assemblages occurring in the fine plus very fine (120 + 230 mesh) sand fractio n of samples from t i l l s of the Saginaw and Lake Michigan lobes. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. B io tite • Saginaw lobe □ Lake Michigan lobe • • •••* lornblende Magnetite. a □□ □ • □ □ C P • • G a rn e t Figure 17. Continued. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 55 characterized by garnet/epidote ratios ranging from 1:1 to 3:1 and the Saginaw and Erie lobe t i l l s were reported as having ratios varying from 3:1 to 4:1. Utilizing the method of Bleuer (19 75) on till samples from southwestern Michigan, heavy mineral analysis was performed and a boun dary was established between the Lake Michigan lobe and the Saginaw lobe in the interlobate area of Kalamazoo County, Michigan (Fig. 18). Data from this analysis may be found in Table 1 of Appendix I. Comparison of the interlobate line based on garnet/ epidote plus hornblende ratios with Shah's interlobate line (1971) based on the morphology of weak morainal ridges (Fig. 18) show marked sim ila rity . However, the more e a s t ward position of the interlobate line based on heavy min eral ratios, such that it includes completely that portion of the Tekonsha moraine considered as a Lake Michigan lobe deposit, seems more realistic than splitting the moraine, as does Shah's in terlo b ate boundary (Fig. 18). Statistics were performed on all heavy mineral data (Appendix II). Chi Square Test indicates that the garnet/ epidote plus hornblende ratio of the sample population from each lobe is not normally distributed (see Fig. 19 and Appendix II ). The Mann-Whitney U Test (Table 9 of Appendix II) shows that the sample population from each lobe is independent and significant at the 0.010 level. The Student T Test (Table 12 of Appendix II) illustrates Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 5 6 Kalamazoo Co Van Buren Co. Calhoun Co. Valparaiso moraine Kendall moraine Kalamazoo moraine Sturgis moraine 1 Tekonsha moraine Interlobate boundary of Shah, 1971 Interlobate boundary based on X-ray diffraction data Interlobate boundary based on heavy mineral data Figure 18. Map of the study area showing morainal deve lopment (grey), and interlobate boundaries based on garnet/ epidote+hornblende ratios (dashed line), X-ray diffraction analysis of 7A/10A peak-height ratios (dotted line) , and the morphology of weak morainal ridges developed by the Lake Michigan lobe (solid line, from Shah, 1971). Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 57 that the difference in the mean garnet/epidote plus horn blende ratio for each lobe is significant at the 0.005 le v e l. Xa 16 - Xb 14 - Saginaw lobe 12 _ Lake Michigan lobe 10 - y Mean Lake Michigan A a lobe Xb Mean Saginaw lobe u. 6 - 4 _ Xa Xb GARNET/EPIDOTE & HORNBLENDE RATIO Figure 19. Histogram of garnet/epidote+hornblende ratios from till samples of the Lake Michigan and Saginaw lobes illustrating the mean garnet/epidote+hornblende ratio for each gro.up of samples (Xa, mean Lake Michigan lobe = 0.166; Xb, mean Saginaw lobe = 0.338). Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. X-ray Diffraction of Clays The use of X-ray diffraction techniques to differen tia te g lac ia l d r if t has been investigated in numerous studies. Frye (1968), in studies published by the Illinois Geological Survey, discussed the utilization of data de rived from clay-mineral studies of drifts of differing ages and areal extent. Castillion (1972) located an inter lobate contact between two surficial tills in Illinois partially by the use of clay-mineral data. In Michigan, Rieck (1976) made use of 7A/10A peak-height ratios to d istin g u ish t i l l s of Saginaw lobe and Huron-Erie lobe provenance. Modifying the methods of Rieck (1976), Glass (1976, personal communication), and Gluskoter (1967), X-ray dif- fractograms (Fig. 20) of basally-oriented clays were ob tained using a Norelco, water cooled, X-ray diffractometer. Glycolated samples were run from 2° to 30° 29. Copper K-alpha radiation and a nickel filter were used. Subse- O 0 quently, peak-height ratios of 7 A and 10A peaks were de termined (Table 1 of Appendix I) and an interlobate boun dary established within the study area (Fig. 18). Chlorite, illite, kaolinite, and vermiculite comprise the major clay minerals in the samples. It is assumed that Q the intensity of the 10A peak was produced by illite. The 58 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 10A 7A 10A 1a 2a 3a 3b1 15a 16b 17 Figure 20. X-ray diffractograms of surface till samples from the Lake Michigan and Saginaw lobes showing the 7A and 10A peaks produced by clay minerals (see Fig. 10 and Table 1 of Appendix I for the location and glacial lobe designation). Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 60 7A 10A 7A 10A 30b 30c 31a 31b 32a 32b 32c 32d Figure 20. Continued, Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 7A 10A 47a 34a 36b 47b^ . 48 ^ 37a 49 38 39 40 53 54 43a 55 43b< 56 57 44a 45 58 46a' Figure 20. Continued. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. o 7A 10A 7A 10A 6 2 64a 60a 67 60b 70 \\ 62 'S~ " A A 63 Figure 20 . Continued. Reproduced with permission of the copyright owner. Further reproduction prohibited wi without permission. o 7A peak was produced either individually or by a combina tion of chlorite, kaolinite, and/or vermiculite. Rieck (1976), in delineating tills from southeastern Michigan, obtained similar results. He stated that "the 7A/10A ratio is not a complete mineralogical characterization but is only used to group samples investigated." Thus, be cause a ratio of the intensities was used and these inten sities were observed on the same diffractogram, comparison between different diffractograms can be performed without 16 “ I Xa Saginaw lobe 14 - Lake Michigan lobe 12 - Xb Mean Lake Michigan lobe Xa 10 - u> Mean Saginaw lobe Xb 8 - o £111 u. 6 — 4 - 2 - I f t ‘ 6 7 i l .8 ' J i ' l!o ' l!l ' l' X-RAY 7A/10A PEAK-HEIGHT RATIO Figure 21. Histogram of 7A/10A peak-height ratios from X-ray diffractograms of samples from Lake Michigan and Saginaw lobe deposits showing the_mean 7A/10A peak-height ratio in each group of samples (Xa, mean Lake Michigan lobe = 0.766; Xb, mean Saginaw lobe = 0.888). Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. using an internal standard (Rieck, 1976). All data was statistically analyzed (see Appendix II) The Chi Square Test indicates that the 7A/10A ratios for the sample populations from each lobe are not normally dis trib u ted (Fig. 21 and Appendix I I) . The Mann-Whitney U Test (Table 8 of Appendix II) indicates that the samples from each lobe are independent at the 0.01 level. Student T Test illustrates that the difference in the mean 7A/10A ratio for each lobe is significant at the 0.005 level (Table 11 of Appendix II). Relationship of Bedrock Geology to Mineral Content in Local Tills The composition of a till is greatly influenced by the composition of the local underlying bedrock. Commonly greater than 50 percent of the bulk mineral content of a till may be representative of the composition of the bed rock beneath it. This is not true of tills found within the study area. As evidenced by the heavy mineral suites from the 120 and 230 mesh sands of till samples collected in the study area, the mineral content of tills within the study area is largely derived from sources outside its boundaries. Large quantities of igneous and metamorphic boulders, cob bles, and gravels also indicate sources foreign to the study area. This is more easily understood when it is ob- Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 6 5 served that an estimated 90 percent of the study area is underlain by the Mississippian Coldwater Shale. According to Anderson (1957), who examined the pebble and sand lithologies of samples from the axial portion of several major Wisconsinan glacial lobes within the Central Lowlands province, the sand fractio n of the Saginaw lobe samples contain 34.4 percent Paleozoic lithologies and 10.6 percent Precambrian lithologies. Lake Michigan lobe samples show 84.5 percent Paleozoic and 4.2 percent Pre cambrian lithologies. Within the pebble fraction, the Saginaw lobe contains 39.1 percent Precambrian and 60.9 percent Paleozoic lithologies. Of the Paleozoic lithologies, the Mississippian Marshall Sandstone constitutes approxi mately 3.6 percent. The Lake Michigan lobe pebble litho logies consist of 10.7 percent Precambrian and 89.3 percent Paleozoic rocks. The lithologic indicators point to an eastern source for both lobes. Anderson (1957) postulated a Huronian source for both lobes. He stated, however, that the Lake Michigan lobe has fewer Huronian rocks as it appears to have by-passed the main Huronian source area of Lake Huron and acquired more granitic material farther northwest. A Huronian provenance for Saginaw lobe tills is more conclusively established by the presence of jasper conglomerate and rare pebbles of the Precambrian Gowganda tillite (Slawson, 1933) which are commonly associated with Saginaw lobe deposits. As demon- Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 66 stxated by Slawson (1933), the source of the jasper con glomerate is localized in the Bruce Mines area (Fig. 22). The location of this jasper conglomerate in the Bruce Mines area brings it to the axis of the Lake Michigan and Lake Huron lobes such that most fragments from this area were transported by the Saginaw lobe of the Huronian ice. It should be noted, however, that Lake Michigan lobe ice also transported, at the very least, several of the red jasper conglomerate and the Precambrian tillite erratics. Leverett (1915), T erw illiger (1954), and Shah (1971) a ll reported finding jasper conglomerate in the Kendall moraine considered herein as a Lake Michigan lobe deposit. Fur thermore, this author found boulders of the Precambrian Gowganda tillite in Lake Michigan lobe deposits in Kala mazoo County. Relationship of Bedrock Topography to Morainal Development A moraine, in the strictest sense, is a morphologic feature composed of sediments deposited d ire c tly by active glacial ice. Numerous morainal classifications exist and within each there are a number of morainal types. However, the classification of moraines is beyond the scope of this text and only those moraines deposited within the study area at the margin of an active continental glacier are considered herein. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 67 / / Goulais Bay / / / i I‘ ft Jasper Conglomerate / ; / / / / \\ I ;; '/ft ! * > » i ines '////«-" V/** ------ I ' I 1 1 i ' / ; / " / / / / / //// Jh i ** * Landing //'/ Detroit Chicago^ / / •> r / ' ' / ' ^ - - jt ifr ♦ . * / a'// '////I // / F««W ,Si*!''> /, / , 1 > 5, >> ///.'• / / / / if L • / Hi. / / I I i ' I 1::‘ I I <* ' ''y// ' / I L !i * * 1 *+ +* * 111 i / / , / *' •/ / / + *; /1 ^ / ♦ i l l + + f / t I I 1 ' * .V / III I'* 'n | * / ' / ; < , ,! i v / * v / I \v v i i , ^ / / < \ ! • » / #! * ^ •<11 \ 'v / 1 'jk * * * / / * / ! * ? /I * / / * / / / / /^Columbus I \ , t I • * I / / / I J' It I * JL i_J ______!L^______* _ +* + i______£___ /■ ------ Figure 22. Map o£ ice flow directions during the Wiscon- sinan glaciation of North America showing the provenance and possible movement directions of the jasper conglomerate er ratics associated primarily with Saginaw lobe tills (after Leverett and Taylor, 1915, in Slawson, 1933). Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 68 The Saginaw and Lake Michigan glacial lobes may be regarded as independent ice flows of the major Wisconsinan continental glacier; each being greatly, though not to tally, controlled by bedrock topography (Anderson and Hor- berg, 1956). The position of ice centers, configuration of ice sheets, and deflection by adjacent glacial lobes is of secondary importance (Anderson and Horberg, 1956). Morainal development may occur when the ablation rate, or rate of back wasting by melting and ablation, approxi mately equals the rate of forward movement of the ice. The net result being a stationary ice front. At such a sta tionary ice front, the forward movement of the ice con tinually brings glacial drift to the terminus where it is released from the ice, forming a moraine (end moraine). The topographic expression of an area may influence morainal development. A topographic high or low, as well as a sharp break in slope may impede the forward movement of glacial ice and effect deposition of drift if the land- form acts as a b a rrie r to forward movement. Shah (1971) postulated th a t., the general northwestward slope of the bedrock surface in southwestern Michigan toward the Lake Michigan lowland may have promoted movement of Lake Michi gan lobe ice toward the east and southeast. The re su lt of such movement being enhanced glacial modification of exis ting bedrock topography. Similarly, the effectiveness of erosion by Saginaw lobe ice may have been lessened when Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 69 encountering the bedrock highland in the southeastern portion of the area (Shah, 1971; Fig. 23). Comparison of the bedrock topography to the d i s t r i bution of moraines in southwestern Michigan (Fig. 24) illustrates the relationship of bedrock topography and morainal development. Note the position of the Kalamazoo moraine (K) of the Saginaw lobe located in the northeast corner of the study area, and the Tekonsha moraine (T) in the eastern portion of the study area. Both moraines are located on topographic ridges. The Sturgis moraine (S) on the border of Cass and St. Joseph Counties is illustra tive of bedrock valley or depression control while the Kalamazoo moraine of the Lake Michigan lobe shows morainal development with "ridge control" in its southwestern por tion and "valley and slope break control" as the moraine extends northeastward. In comparing the relationship of bedrock topography to the distribution of Wisconsinan moraines in southwestern Michigan, the effect of pre-Wisconsinan glaciation should be considered. Assuming, therefore, that bedrock topo graphy influences morainal development, sequential glacia tion should result in a repetition of morainal development. Thus, although Wisconsinan ice may not have actually con tacted true bedrock, the influence of bedrock topography on Wisconsinan morainal development may have been trans mitted, at least partially, through prior glacial landforms. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. ALLEGAN BARRY' ATOI 7 SO t NORTH BUREN1 CALHOUN ■Bso , *oq ----( CA8S ST JOSEPH O/. l" m iles \ Figure 23. Map showing the bedrock topography of southwestern Michigan (modified from Shah, 1971). Study area heavily outlined. EATON EATON CO BRANCH BRANCH CO KALAMAZOO 6o°'' ST JOSEPH CO --- J ALLEGAN CASS CO BERRIEN BERRIEN CO Valparalao Moraine Tekoneha Moraine Kalamazoo Moraine Sturgla Moraine Kendall Moraine S tudy area Figure 24. Map illustrating the relationship of bedrock topography to morainal de gan Geological Survey, 1975). velopment (shaded) in southwestern Michigan (modified from Shah, 1971, and the Michi Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Deglaciation of the Study Area At the beginning of deglaciation of southwestern Michigan and the study area, Saginaw lobe ice extended slightly south of the Michigan-Indiana border, while Lake Michigan lobe ice was well contained in its basin to the west. As the Lake Michigan lobe advanced slowly to the south-southeast, Saginaw lobe ice retreated to the posi tion of the Sturgis moraine in St. Joseph County, Michigan (Fig. 25). Shah (1971) sta te d that when the Saginaw lobe was in this position, it deposited the Alamo and Kendall moraines in northwestern Kalamazoo and northeastern Van Buren Counties. With additional retreat of the Saginaw lobe and continued advance of the Lake Michigan ice, Shah (1971) further postulated that the Lake Michigan lobe overrode the Kendall and Alamo moraines while advancing to and stagnating at a position near the present main axis of the Kalamazoo moraine. T ill samples collected on the Kendall and Alamo moraines were analyzed using X-ray dif fraction and heavy mineral suites as previously described. The results indicate that the Kendall and Alamo moraines are deposits of the Lake Michigan lobe. Thus, when the Saginaw lobe was positioned at the Sturgis moraine in St. Joseph County, the Lake Michigan lobe probably was at or near the present Kalamazoo moraine in Kalamazoo and Cass C ounties. 72 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. .7.3 Following the formation of the Sturgis moraine in St. Joseph County, the Saginaw lobe continued its retreat leaving a series of till and outwash plains (Tig- 25). At the position of the Tekonsha moraine the Saginaw ice hal ted to develop a strong recessional moraine. The Lake Michigan lobe, however, began to advance from its position near the Kalamazoo moraine, overriding it and pushing its way toward the western border of the present Tekonsha moraine. At this position the Lake Michigan ice deposited the northeast-southwest trending arm of the Tekonsha mor aine and began or continued development of the Sturgis moraine in western St. Joseph County and eastern Cass County. Contemporaneous with the above is the development of weak morainal ridges in Saginaw lobe sediments which Shah (1971) defined as the outermost limit of the Lake Michigan lobe in southwestern Michigan (Fig. 9). Overriding of the Kalamazoo moraine is supported by several lines of evidence. First, the presence of ablation t i l l from the Lake Michigan lobe over the Kalamazoo moraine implies that ice passed over the moraine and at some point became stationary and melted lowering the ablation t il l to the surface. Second, Shah (1971) reported the presence of thin till plains over outwash plains in Cooper and Prairie Ronde Townships of Kalamazoo County. This implies a rapid retreat of a thin sheet of ice leaving ground moraine (Fig. 25). Third, the presence of weak morainal ridges (push Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 45b miles 1 m , Explanation D«ltoe End moraine E skers Ground moraine Outwash Thin till on outwash Drumlins I nsx IX MHA IZ1 IZ1 | | | Lake I- beds and I drainage Clay capping ways on outwash 95J Sand dunes Figure 25. Surface geology of southwestern Michigan (after Shah, 1971) showing Wis consinan glacial deposits (V, Valparaiso moraine; K, Kendall moraine; Ka, Kalamazoo moraine; T, Tekonsha moraine; S, Sturgis moraine). Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 75 moraines of Shah, 1971) east of the Kalamazoo moraine which parallel other known moraines of the Lake Michigan lobe and possibly indicate glacial surges resulting from differential flow-lag. Fourth and last, folding occurs in the drift material of the Kalamazoo moraine (Fig. 26). Such folding indicates overriding of the moraine and sub sequent deformation of the underlying drift resulting from stresses imparted by the moving ice. With the ice fronts of both lobes standing at their respective positions of the Tekonsha moraine, melt-waters Figure 26. Photograph of a fold occurring in the d rift of the Kalamazoo moraine of the Lake Michigan lobe indi cating the overriding and deformation of the moraine by Lake Michigan lobe ice in Wisconsinan time (photograph taken by W. T. Straw, 1973, on the campus of Western Michi gan University). Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 76 from both lobes combined with melt-waters from the Erie lobe ice to form the Kankakee Torrent (Fig. 7, see pre vious discussion). The Kankakee Torrent discharged to the southwest as an ice marginal stream bordering the Lake Michigan lobe ice. A slight readvance of the Saginaw lobe is indicated by drumlins and a thin ablation t i l l on the northwest- southeast trending Tekonsha moraine. The ice front ad vanced at least as far as the drumlin field southeast of Kalamazoo County. The small morainic forms extending northwest from Bronson Township in Branch County (T7S,R8W) may represent the outer limit of this oscillation. As the Saginaw lobe retreated rapidly back to the Tekonsha moraine, the Lake Michigan ice retreated slowly westward toward the Kalamazoo moraine. Oscillation of the Lake Michigan ice front is marked by thin linear moraines in Prairie Ronde, Portage, and Cooper Townships of Kala mazoo County. The Saginaw lobe continued its retreat from the Te konsha moraine slowly to the position of the northwest- southeast trending Kalamazoo moraine. With both lobes stationary at their corresponding Kalamazoo moraine, a period of standstill resulted in the massive morainic system of today. Continued westward retreat of the Lake Michigan lobe ice resulted in deposition of the Kendall, and later, the Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Valparaiso morainic system previously discussed. The history of the Saginaw and Lake Michigan lobes outside of the study area through the remainder of their retreat during Wisconsinan time is generally described in Leverett and Taylor (1915). References discussing the deglaciation of Michigan during Wisconsinan time include the following: Dorr and Eschman (19 71), Eschman and Farrand (19 74), and Wayne and Zumberge (1965). SUMMARY AND CONCLUSIONS Tills within the study area are generally poorly consolidated, although compact tills may be found in lo calized areas or at depth. Gravels are common and a wide range of lithologies are represented, the majority being derived from Canadian Shield bedrock sources. The effect of local bedrock on the composition of t i l l within the study area is markedly lessened because ap proximately 90 percent of the study area is underlain by the Lower Mississippian Coldwater Shale. Heavy mineral suites in the 120 and 230 mesh sands also are reflective of a Canadian Shield provenance. Morainal development shows a strong correlation with bedrock topography in the study area. The Kalamazoo and Tekonsha moraines of the Saginaw lobe are located on bed rock highs. It is possible that forward movement of the Saginaw ice was impeded by these bedrock highs and resulted Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 78 in the deposition of the present-day morainal systems. The Sturgis moraine in Cass and St. Joseph Counties is located in a bedrock low. Argument is made that any break in slope may halt the forward movement of a weak ice front and, thereby, "trigger" the deposition of t i l l and subse quent morainal development. The deglaciation of Michigan in Wisconsinan time left the state covered with the present-day glacial landforms. While the history of deglaciation in the past has been based primarily on morphologic evidence (the morainal systems) and has dealt with broad regional areas, recent studies have turned to a more detailed description of localized areas. Analytical techniques have been developed and utilized which allow the discrimination of glacial sediments with differing source areas. These techniques have proven particularly effective in areas of glacial lobe convergence. Portions of five C5) morainal systems are found in the study area. Lake Michigan lobe ice is responsible for part or all of the Valparaiso, Kendall, Sturgis, and the northeast trending Kalamazoo and Tekonsha moraines. The Saginaw lobe developed the northwest trending arms of the Kalamazoo and Tekonsha moraines and a portion of the Stur gis moraine in St. Joseph County and eastward. The interplay of the Lake Michigan lobe and Saginaw lobe ice in southwestern Michigan resulted in the develop- Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 79 ment of a classic interlobate area. In the past, mor phologic characteristics of the area have been utilized to describe the character and relationship of the ice fronts during deglaciation. In the present study, tex tural and mineralogic parameters are used to enhance the knowledge of the interlobate boundary relationship of the Lake Michigan and Saginaw lobes in Kalamazoo County, Michigan. Results using textural and magnetic susceptibility data to delineate tills of the Lake Michigan and Saginaw lobes are inconclusive. Marked variability in till texture in localized areas precludes any textural correlation on a regional scale. A ratio of percent sand/percent mud, however, shows that Lake Michigan lobe tills have a s ta tis tic a lly higher clay content than Saginaw lobe tills . The inconclusive nature of results from magnetic suscep tib ility analysis cannot be singularly explained. It is hypothesized that either the results are truely incon clusive, or the mixing of tills by the interplay of the two ice lobes and weathering, either singularly or in combination, resulted in poor magnetic susceptibility measurements. An interlobate boundary relationship is established using differences in ratios of heavy minerals and clay mineralogic data. Comparison of the interlobate boundaries using the above methods with Shah's interlobate boundary Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 80 (1971) based on the morphology of weak morainal ridges shows similar results. However, the position of the in terlobate boundary further to the east, as defined in this study, appears more reasonable as it includes the entire northeast trending limb of the Tekonsha moraine. Suggestions for Future Research The use of heavy mineral suites to delineate tills of differing provenance has been established in past lite ra ture. Although heavy mineral separations often prove to be tedious and time consuming, the results from such data are the least effected by outside variables such as wea thering, etc. It is therefore suggested that future re search in delineating t i l l by provenance consider the use of heavy mineral analysis as an especially viable tool. Field observations and literature review characterize the morainal deposits within the study area as containing relatively large amounts of stratified drift. Attention should be given this fact and a detailed study of the proportions of stratified and unstratified drift embodied by the moraines of the area is recommended. Such a know ledge would greatly add to the understanding of morainal development within the study area. As it is questioned whether the weathering of tills and the mixing of t ills within the study area are singu larly or jointly responsible for inconclusive magnetic Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 81 susceptibility analysis, attention should be given to the effects of weathering and mixing on analytical techniques used to delineate tills of differing provenance. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. REFERENCES 82 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. REFERENCES CITED Anderson, R. C., 1957, Pebble and sand lithology of the major Wisconsin glacial lobes of the Central Lowland: G.S.A. Bull., v. 6 8 , pp 1415-1450. Anderson, R. C., and Horberg, L., 1956, Bedrock topography and Pleistocene glacial lobes in the central United States: Jour, of Geol., v. 65, no. 2, p. 101-116. Bleuer, N. K., 1975, The Stone Creek Section: a historical key to the glacial stratigraphy of west-central In diana, Ind. D.N.R. (Geol. Surv.) Occassional Paper 11, 8 p. Bloss, F. D., 1961, An introduction to the methods of op tical crystallography, Holt, Rinehart and Winston, N. Y., 294 p. Boulton, G. S., 1968, Flow tills and related deposits on some Vestspitsbergen glaciers: Jour, of Glaciology, v. 7, no. 51, p. 391-412. 1970b, The deposition of subglacial and melt-out til l s at the margins of certain Svalbard glaciers: Jour. Glaciology, v. 9, no. 56, p. 231-245. 1970, On the origin and transport of englacial debris in Svalbard glaciers: Jour, of Glaciology, v. 9, no. 56, p. 213-229. 1971, Till genesis and fabric in Svalbard Spitsbergen in Goldthwait (Ed.): T il l : A Symposium, 1971, Ohio State University Press, Columbus, Oh., p. 41-72. 1972, Modern Arctic glaciers as depositional models for former ice sheets: Geol. Soc. London, v. 128, p. 361-393. Breene, V. M., 1957, Preliminary study of the heavy min erals in the Wisconsin and Illinoian t il l s near Cin cinnati, Oh., The Compass of Sigma Gamma Epsilon, v. 34, no. 2, p. 132-153. Broecker, W. S., and Farrand, W. R., 1963, Radiocarbon age of the Two Creeks Forest bed, Wisconsin: G.S.A. Bull, v. 74, p. 795-802. 83 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Brophy, J. A., 1959, Heavy mineral ratios of Sangamon weathering profiles in Illinois: 111. State Geol. Survey Circ. 273, 22 p. Castillion, D. A., 1972, The relationships between morpho- stratigraphy, rock stratigraphy, and aspects of till fabric in central Illinois (unpub. Ph.D. dissertation) M.S.U., East Lansing, Mi., 149 p. Chamberlin, T. C., 1883a, Geology of Wisconsin: Wisconsin Geol. Nat. History Survey, v. 1, p. 1-300. 1883b, Terminal moraine of the second glacial epoch: U.S. Geol. Survey Third Ann. Rept., p. 291-402. 1894, Proposed genetic classification of Pleistocene glacial formations: Jour. Geol., v. 2, p. 517-538. 1895, Glacial phenomena of North America: p. 724- 775 in Geikie, J ., The Great Ice Age, 2nd ed ., Apple ton, N. Y. Charlesworth, J. K., 1957, The Quaternary Era, with special reference to its glaciation: Edward Arnold, London, 2 v . , 1700 p . Derry, D. R., 1934, Heavy minerals of the Ordovician sedi ments of Ontario: J.S.P., v. 4, no. 2, p. 83-88. Dorr, J. A. J r ., and Eschman, D. F., 1971, Geology of Michi gan, Univ. of Mich. Press, Ann Arbor, Mi., 476 p. Dreimanis, A., 1971, Procedures of t i l l investigations in North America: a general review, in Goldthwait (Ed.), 1971, Till: A Symposium, Ohio State University Press, Columbus, Ohio, p. 2 7-40. Dreimanis, A., and Reavely, G. H., 1953, Differentiation of the lower and upper t i l l along the north shore of Lake Erie: J.S.P., v. 23, p. 238-259. Dreimanis, A., et a l., 1957, Heavy mineral studies in tills of Ontario and adjacent areas: J.S.P., v. 27, no. 2, p. 148-161. Dreimanis, A., and Vagners, U. J ., 1971, Bimodal distribu tion of rock and mineral fragments in basal t il l s , in Goldthwait (Ed.), Till: A Symposium, Ohio State Uni versity Press, Columbus, Ohio, p. 237-250. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Dreimanis, A., and Vagners, U. J ., 1972, The effect of lithology upon texture of t i l l , in Goldthwait (Ed.)? 1972, Glacial Deposits, Benchmark Papers in Geology, v. 21, Dowden, Hurchinson, and Ross, Inc., Stouds- berg, Pa., p. 86-102. Dreimanis, A., and Morner, N. A., 1973, The Erie interstade G.S.A. Memoir No. 136, p. 107-134. Ekblaw, G. E., and Athy, L. F ., 1925, Glacial Kankakee Torrent in northeastern Illinois: Geol. Soc. Am. B u ll., v. 36, p. 417-428. Farrand, W. R., et al., 1969, Cary-Port Huron Interstade: evidence from a buried bryophyte bed, Cheboygan County Michigan; Geol. Soc. America, Special Paper No. 123, p. 249-262. Farrand, W. R ., and Eschman, D. F., 1974, Glaciation of the southern peninsula of Michigan: A Review, Michi gan Academician, v. 7, no. 1, p. 31-56. Flint, R. F., 1957, Glacial and Pleistocene Geology, John Wiley and Sons, Inc., New York, N. Y., 553 p. 1971, Glacial and Quaternary Geology, John Wiley and Sons, Inc., New York, N. Y., 892 p. Folk, R. L., 1968, Petrology of sedimentary rocks, Hem p h ills, Austin, Tx., 170 p. Frye, J. C., 1968, Development of Pleistocene stratigraphy in Illinois, in the Quaternary of Illinois: Urbana, Univ. of Illin o is, College of Agriculture Spec. Pub. 14, p. 3-10. Frye, J. C., and Leonard, A. B., 1952, Pleistocene geology of Kansas: Kansas Geol. Survey Bull. 99, 230 p. Frye, J. C., Willman, H. B ., and Glass, H. D., 1960, Gumbotil, accretion-gley, and the weathering pro file: Illinois State Geol. Survey Circ. 295, 39 p. Gluskoter, H. J., 1967, Clay minerals in Illinois coals: J.S .P., v. 37, no. 1, p. 205-214. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 86 Goldthwait, R. P., 1971, Introduction to till, today: in Goldthwait ( E d . ) , 197 ^ Till: A Symposium, Ohio State Univ. Press, Columbus, Ohio, p. 3-26. Goldthwait, R. P., (Ed.), 1975, Glacial deposits, Benchmark Papers in Geology, v. 21, Dowden, Hutchinson, and Ross, Inc., Stoudsberg, Pa., 465 p. Gravenor, C. P., 1951, Bedrock source of t il l s in south western Ontario, Am. Jour, of Science, v. 249, p. 66-71. Gravenor, C. P., and Stupavsky, M., 1974, Magnetic suscep tibility of the surface tills of southern Ontario: Canadian Journal Earth Sci., v. 11, no. 5, p. 658-663. Gravenor, C. P., et a l ., 1976, Technique for measurement of isotropic magnetic susceptibility of t i l l : G.S.A. Bull, v. 87, p. 818-820. Holmes, C. D., 1941, Till fabric: Geol. Soc. Am. Bull., v. 52, p. 1299-1354. Hough, J. L., 1958, Geology of the Great Lakes, University of Illinois Press, Urbana, 111., 313 p. Ibrahim, Abdelwahid (Wahid), 1969, Ground water exploration in Kalamazoo County, Michigan utilizing the geophysical method: unpub. Ph.D. dissertation, Michigan State University, East Lansing, Mi., 125 p. Jones, R. L., and Beavers, A. H., 1964a, Magnetic suscep tibility as an aid in characterization and differen tiation of loess: J.S.P., v. 34, p. 881-883. Kruger, F. C., 1937, A sedimentary and petrographic study of certain glacial drifts of Minnesota: Am. Jour. Sci., 5th s e r . , v. 34, p. 345-363. Krumbein, W. C., 1933, Textural and lithologic variations in glacial till: Jour, of Geol., v. 41, p. 382-408. Krumbein, W. C., and Graybill, F. A., 1965, An introduction to sta tistic a l models in geology, McGraw Hill Book Co., New York, N. Y., 475 p. Krumbein, W. C., and Pettijohn, F. J ., 1938, Manual of sedi mentary petrography, Appleton-Century-Crofts, Inc., New York, N. Y., 549 p. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 87 Kuenzi, W. D. , 1974, unpublished laboratory notes, Western Michigan University, Kalamazoo, Mi. Kunkle, G. R. , 1963, Lake Ypsilanti: a probable late Pleistocene low-lake stage in the Erie Basin: Jour, of Geol., v. 71, p. 72-75. Leighton, M. M. , 1960, The classification of Wisconsin glacial stage of the northcentral United States: Jour. Geol., v. 6 8 , p. 529-552. Leverett, F., and Taylor, F. B., 1915, The Pleistocene of Indiana and Michigan and the history of the Great Lakes, U.S. Geol. Surv. , Mon LIII, 529 p. Malanchak, J. E., 1973, Geology of Atwater well field, Kalamazoo County, Michigan, unpubl. Masters Thesis, Geology Dept., Western Michigan Univ., Kalamazoo, Mi. Mendenhall, W. , 1975 , Introduction to probability and s ta tis tic s , 4th Ed., Wadsworth Publ. Co., Inc., Bel mont, C alif., 460 p. Nagata, T ., 1961, Rock magnetism, Maruzen Co. Ltd., Tokyo, 350 p. Rieck, R. L., 1976, The glacial geomorphology of an in te r lobate area in southeast Michigan: relationships be tween landforms, sediments, and bedrock, Unpubl. Ph.D. dissertation, M.S.U., East Lansing, Mi., 216 p. Shah, B. P., 1971, Evaluation of natural aggregates in Kalamazoo County and vicinity, Michigan, Unpubl. Ph.D. dissertation, Dept, of Geol., Michigan State Univ., East Lansing, Mi., 193 p. Simonson, R. W., 1954, Identification and interpretation of buried soils: Am. Jour. Sci., v. 252, p. 705-732. Sitler, R. F., 1963, Petrography of till from northeastern Ohio and northwestern Pennsylvania: J.S.P., v. 33, no. 2, p. 365-379. Slawson, C. B ., 1933, The jasper conglomerate, an index of drift dispersion: Jour. Geol., v. 41, p. 546-552. Spence, J. T ., et a l., 1960, Elementary s ta tistic s , Apple- ton-Century-Crofts, New York, N. Y., 245 p. Terwilliger, F. W., 1954, The glacial geology and ground water resources of Van Buren County, Mi.: Michigan Geol. Survey Occassional Paper 48, 95 p. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 88 Thorp, James, et a l., 1951, Some post-Pleistocene buried soils of central United States: Jour. Soil Sci., v. 2 , p t . 1 , p . 1-19. Vonder Haar, S. P., and Johnson, W. H., 1973, Mean magnetic susceptibility: a useful parameter for stratigraphic studies of glacial till: J.S.P., v. 43, p. 1148-1151. Wayne, W. J ., and Thornbury, W. D., 1965, Wisconsin stra tigraphy of northern and eastern Indiana: Ind. and Ohio Geol. Surveys, 5th Biennial Pleistocene Field Conf. Guidebook, p. 1-34. Wayne, W. J . , and Zumberge, J. H., 1965, Pleistocene geology of Indiana and Michigan, in Wright, H. E., and Frey, D. G., (Ed.), The Quaternary of the United States, Princeton Univ. Press, Princeton, N. J ., p. 63-84. Willman, M. B., and Frye, J. C., 1970, Pleistocene s t r a t i graphy of Illinois: 111. Geol. Surv. Bull. No. 94. Winchell, A., 1961, First biennial report of the progress of the Geological Survey of Michigan, embracing ob servations on the geology, zoology, and botany of the lower peninsula: Lansing, Hosmer and Kerr, 339 p. Zumberge, J. H., 1960, Correlation of Wisconsin drifts in Illinois, Indiana, Michigan, and Ohio: G.S.A. Bull., v. 71, p. 1177-1188. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. APPENDIX I 89 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. o Ratio Sand/Mud . 008 . 1. 891 1. 1.191 573 7. 1 1.293 1.164 0. 511 0. 732 0. 10. 574 10. Provenance Lobe L L 2.416 L L L L S L XAL ecn Mud Percent 11. 78 11. 57.72 49. 79 49. 43.60 46.20 Sand Percent 70. 7370. 29.27 89. 22 89. 50.21 56.40 53. 80 53. 33. 83 33. 66.17 42.28 65.42 34.58 L aE + Hbd + Ga/Ep - 210 . . 0.144 0 0.210 0.144 0.24353 54. 77 45. 0.207 0.295 0.125 91.36 8.64 ek Height Peak 8 7A/10A 7A/10A - 0.400 748 . 0 0.611 0.288 0. 793 0. n X i i • o • .20 u bo U) u 3 bfltH aS S 2.49 2 .70 2 796 0. 2 5.45 0.661 2.42 1.74 0.579 1.65 4.00 1.06 4.30 0.721 (grams) .00 Bulk Wt. Wt. Bulk 201.00 203.10 202.40 210 216.00 203.00 Range 12W 203.60 12W 10W 11W 198.00 11W 205.00 11W 11W 212.80 2.84 11W 12W Township 2S 2SW 12 2S 2S 2S IS IS IS Section 9 21 20 27 13 2S 30 gravel fraction; S, Saginaw lobe; L, Lake Michigan lobe; A, anomaly; 0, epidote + hornblende ratio data (symbols: outwash; Ga, garnet; X, X-ray; Ep, H, heavy epidote; minerals; Hbd, hornblende) B, bulk weight, defined as the sample weight of the original sample minus the / Section 1/4 SW SW SW NE station . SW 25 . . . NE 7. NW 19 8 2 5. NE 1 4. 6 Sample 3c. SW 9 3a. SW 9 2S 3b. TABLE 1. TABLE Location, textural, magnetic susceptibility, X-ray diffraction, and garnet/ Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. without prohibited reproduction Further owner. copyright the of permission with Reproduced TABLE 1. Continued. qoag g a o iq o u qqgT S fr.0T XsSo 3 3 t r e i i 9 A o . i < 2 on ‘§bh *osns diqsuMOj, pnH/puts ' a TM w UOIlBiS U0T138S 8 lUOD-IScf (sureuS) VOI/VZ spduins H sSUBtf puts sqoq p/i t • * 3 ^ M C l T C H t H r H r M C M C H i M C o H r o H r o t o O © © O M C © M C CO M C M C M C O to o o o O L o © © © CO O o o o o o o t O L • • • • • • • • • • • • • • • • • • * • • • • • • • • • • • # • • • • • • • • • i — r > o © o \ © o o © O O o M C © H r o t 2 M C M C M C o o O O L O o © © O L O L O L H r o s OC OC CO CO CO CO CO o # 3 5 O C M C ^ * r H r M C o M C 3 - r H r H r H r M C 3£ M C oto to o t o O L o t O to 0 0 H r © 2 0 0 H r W © m : H t o t M C M C O M C O M C H r o © O L O L O M C H r H r M C M C HrH r M C -H T o o o O L o ^ * r H r M C O C 2 ■^3" W • • # H r © © M C M C O L O L o t * > [ H r O O H r O C M C 0 0 h ^ 2 M C M C © O L o o 0 0 M C M C to H r to c/5 J • • 1 6 • • © o CM C 1 i © o t o O L H r M C H r © o © O L H r O C 0 0 M C H r to o H r w 2 3 vO (NI vD H r O L M C o o t^- ■=» ^ O cd © H r O L M C O v M C O 1LO L —1 T ■*3- © i O o H r H r H r *5»* O O © O L O M C H r © © H r © W 2 W © o t © O L M C o t H r o oto t to to CO H r CO M C o H r o 0 0 o . ^ r r>* O L cd • « • • • • • • • • © M C 0 0 O L ■'=3* " 3 ^ P2 - 3 ^ O C H r O L o o H r H r H r H r M C H r © o t O C © H r 0 0 H r O L to H r • • • « O L < O L o o t o t 0 0 H r © H r © M C M C © H r M C CO O L X * 3 ^ H r ^ r CO O o to 0 0 M C © • • • • 18a. SW 23 3S 8 W 210.20 3.85 0.786 0.336 56.80 43.20 XAS 1.314 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. without prohibited reproduction Further owner. copyright the of permission with Reproduced TABLE 1. Continued. pqH dg/ng + quao-iagpn^ oqo t/T uoxqoos qqSiOH aouBTioAoaj § ^0 X ^.01 s§3 •osns pnw/ptres diqsuMOj, uoiqeqs uoiqoss quaojoj TM ^Iing (suinaS) VOT/VZ aiduiBs oSUB^I puns aqoq *§ bj ^ X co to o X> CD x < CO CD CD CD a* O v vO < CO l C H r w H r . ^ r . ^ r M C o o o i c O L o a* a* i c X H r o H r to o 2 o t M C l C l C o O H r o l C o to O L O L OC CO CO CO • • • • • • • • • • • • • • • • • • • • • o M C * a £ 2 H r o t o oo - a o H r H - r 0 0 * a CM rH CO 2 W w O L o o o O L o t i o i c T—i o t O • • • CM CM XI ^ t ^ r ^a- H r CM l C H r M C M C M C M C O L - a - a - a O O L 0 0 o o H r - a M C OCO CO H r H r M C t a* - a 0 0 H r H r VO LO x r 0 0 H - 00 M C M C M C H r H r = 3 M C M C H r 0 0 H r H r H r co H r O H r a* *ci c a* LO to XI O L S OCO CO o O o O O a c • i x O v CM M C i H r T r^. O o t vO i c vO IXJ XI H r l o to - a M C o O 2 » g H r H r 0 0 H r y g M C O l C o t H r H r H r ! — — vo o I • • • : ! O V a* o t W CM rH H r —! - P X i— M C - a 0 0 O O C H r o O Cl o t CM LO - a rH . s C M C O L OCO CO CO to o O L o 0 L • • • • • • M C O O v a* - a H r O M C M C s - C H r H - r M C O L OO LO LO IX XI O L H r H r fv. O L o o t a* O L O L to x e M C M C O O H r i — r H r o t y g l C OCO CO 0 0 a c • • • X H r a* o t LO a* o OCO CO w M C H r H r to o ^ r o O 0 0 a* O o O to 0 0 o O L i c l C • • • O V O V rH vO XI O L O L l C - a 0 0 - a M C H r M C M C 0 0 rH O v l C LO 0 0 O L ^ g o t H r H r H r H r l C o t O C O O H r l C CO l • rH CM O v M C - a 0LO 00 LO XI H r O l C l C H r O v 2 » g M C M C o t M C M C o O v M C o * " C l C H r H r O H r CM o t - a CO H r H r O • • : D v - a H r O v 00 CM XI M C oo a* S g»» . ^ E CM o t = 2 O O O 0 0 O H r ^ r H r CO l C O L O o t o t 0 0 • Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. without prohibited reproduction Further owner. copyright the of permission with Reproduced TABLE 1. Continued. q + d3/-BDpqH + oqa t/T uoxqoas n quaoasj pn^ qqStSH >[BSd SOUBUSAOJd S ^O X ^.OI sSo *osn§ pn^/puBS diqsuMOX uoxqBqs uoxqoas TM 3iing qusojiaj (SUTBtS) VOT/VZ siduiBS 9§UBtf OXqBtf pxres aqoq "S bk H t Ci 0 ~ y * y M C O C M C 0 O C - H O O O L O L “ 3 < O O H r 0 O L CM 2 w H t H r CO H r O C 0 co H r O O O H t O C 00 O l • • • • • • • • • • • • • • • • • • • • • • • • • • • : 33 \o vO H t vO vO * ^ c - H M C - H M C H t H t M C M C O O O M C 0 0 X < H r H t rs- M C 0 O C OC CO CO CO to O C O M C D C C/D w • • • • 34 • 0 H t H t 0 0 o c 0 O C H- * ^ c M C O O >H- H c> M C M C vo to i C t to o> 0 to to 0 -3 to o C/D C/D to H es • • • • • • 3 1 H t H t " H O C O L H t ci O L H r M C O L i O to O L i C Ci H* 0 0 M C .0 0 0 H t 3: i C O O C M C O O O O O C to o • • • • 0 0 0 vO H* O L H* M C H t H t H t M C 0 M C 0 o t r*^ H t M C O C 0 O C O C 0 M C to O L O L C/D OC OCO CO CO to CO to o M C CJ • » • • O vO H* t— O L to O C O v O L 1 t— O L 0 O ot oto to to to M C 3 0 0 0 O L O O O L O C O O O H r O C H r O i O O C H t o t H t s a • • • • • • • • • • • • • • • • • 34 1 O H r H r H t vO *r^ r H* 0 r^ to H r oH" to O L O L 0 0 m c vO i * C t * y i C 0 0 0 0 H t H t W i C o t H • 34 • H t O 1 T— H" to vO O 0 0 vO M C O C to H r H t O C 00 M C O O H t to M C M C O O o t O C M C M C M C C c • • • • • • vO M C O r-3 0 0 M C M C 00 M C vO H* O O C H* H t r-* O C H t M C H t O L i C M C O O H t i C OCO CO y* i C O 0 0 M C M C • • • • M C M C ' H o t O C M C O O 0 M C H t O C - H j r M C O L O L M C O O O O L r^- 0 0 © O L M C H t to o t . > ! H r O O • o 00 to M C M C M C 0 0 M C T3 H r M C 3 0 0 i C O L O c^. M C H r to M C CO to O L O M C O M C M C O C co • . 33. NW 28 2S 10W 195.70 3.22 - 0.201 75.14 24.86 L 3.022 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. without prohibited reproduction Further owner. copyright the of permission with Reproduced TABLE 1. Continued. pnp\[ quooaod PQH dg/BQ + qqSiSH 3[B8i uoiqoas OOUBUOAOJCd S fr_0TsSo X •osns pnw/pires , j O M u s q i d • uoxqoos uoiq.Bq.s im quao-iod ( VOI/VZ spduiBS ba ib u s . a w aSuB^ oxq.BH pu^s eqoq *S V/l ) S bjai cn CO — MLO CM T—f © rH OO cn i o t 3= o t CM LO © rH o o T—! © r-H CM rH ocn to o t © o t 1 © © LO r-*H © © © t-H CM MC Mtoto t o t CM © CM rH CM rH CO MC MC CM CM CM CM CO CM CO cn © © © OCM LO O oLO to to • • • • • • • • • » • • • • • • • • • • * • • • • ♦ • • • • • • • • • • • • • • • • • • • • • • • • • • • • • 46 CM CM © o O r-H o © in © to c8 1 i © 2 2= o t o t CM 3 OL © LO LO © CO © o o t o t o t LO I r-H t 1 rH • CM ; CM *3“ rH co © © © OO t © © © © cn © CO y~ © © © © © CM © © © oCM to o t OCO CO H cC • • • • • • • • • • • • • C- © © o t — CM T—I © CM CM rH © rH © © r^. ^3* LO o t Os2 s CO 3 © © o t rH o LO y* CM to o t ^ h LO rH cn cn CM T—1 00 00 H- C- H© rH © © © © O © CM © CM i—! © r-H r-H © o t MC CM CM CM r-H LO OCO CO r-H © © to oto to CtJ h rH © © Mcn CM r—i CO o © © © © © © n**© *3* cn < M© CM © © to cn to r-n to LO I>H ^3^ © © 3^ Or Mr © rH CM rH LO O* LO to to . # # 15 © © O © o t o t o oto to CM © 2 CM © o© to r-H © OCM LO LO o t 00 MC MCM CM CM CM © LO OC CO CO CO oC CM CM to 3 • • • • • * CM i—! LO © © rH w w OCO CO rH CM rH 1—i H©© © rH © © r-H o to c cn to MC CM CM CM © o t < o t © 0t rH to 00 © CO - h OLO OO OLO CO o © © T—1 o t © CM 00 r-n co to M© CM LO HCM rH r-. rH t O © ^ r H© rH o t © 0©© © 00 3 H - CM M© LO CM r—1 cn c r-H rH CM rH rH © © OLO CO 0N 00 3^ rH CM 3 O© LO OCO CO - ^ h o T—1 CO CO rH *3- LO © to LO CM © CM CM CM ^ r © © rH CO LO CM CM 3= © to Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. without prohibited reproduction Further owner. copyright the of permission with Reproduced TABLE 1. Continued. pnj»{ q + <*3/^9PqH + oqa t/l / t uotqoag qqSxaH ^Barf OOUBUSAOtJ s on ‘Sew •osng S pnw/puBS d dxqsuMOX * 0 X _0I t uotqBqs qusotaj uoiqoag im lUODAOJ ( ¥01/VZ apduiBg o o siubjc a w OiqBtf pues aqoq S) O 0 0 H r o o * d * ] N C vO CNJ CM O v O t O L O L o t o t o t M C CO M C CO H r H r •=»■ H r O v 0 0 0 0 o o o » ^ c o c *-3 OC CO CO CO P3 O C M C M C M C o O C O C 49. NW 20 3S 8 W 190.50 2.64 0.865 0.291 75.84 24.16 S 3.139 95 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. without prohibited reproduction Further owner. copyright the of permission with Reproduced TABLE 1. Continued. q + da/BDpqH + qqSxaH 3[B9d uoiqosg uoiqosg soubusaoj § t.0T Xs§3 t *osns pnw/puBs diqsuMOX q.U30A3d uoiqoss UOT TM g W ( VOT/VZ 81 suiba OITBtf 9§UBd dure s pUBS aqoq 3 *S .Bq.S p/i b S) ;^ ^ CM rH CO 3 tH cn CM rH CO O LO cn CM o o o CO rH rH CO rH cn LO to LO vO cn o t © 2 CO o00 to to O o o to X < CO rH OL OL OL OLO LO LO LO LO LO LO LO t t to o t o t to H H ^ • • « • • • • • • • • • • » • • • • • • • • • • • • • • • • « • • • • • • • • • • • • « • • • • 17 • • • • • • • • • • • O vo © no o cn 0CO 00 rH CM 3 o r^. 00 o t o t CO CM T—1 o © rH w s= / 2 C/3 OCO CO ^ r CO LO vO o 10 = Or LO rH vO MLO CM 00 ML ML to LO CM LO CM vD CM MCM CM rH CM CM rH o to to CO o 3 to MtoL © LO o t CM 27 : © rH O O o o o CM LO CO O © LO o CM O rH cn o o t CO CM MLO CM M" jsp o o t o t CM Hoo o rH LO 3 2 OCO CO = m 0 © cn o t rH nCM COcn CO CO o MC CM CM CM CM cn o cn o t LO -^r rH CM rH rH 00 rs- LO 2 ncn cn w w 21 14 cn CO HrH to rH o OrH CO o00 co cn o t to o t CO LO rH 3 nc o t cn cn C/3 OCO CO OC CO CO CO LO 11 £ Hto rH vO CM rH 00 00 CM 00 o to rH o O LO oo O O o o CO 3 = vo CM ■* VO o 00 00 o t cn CO o cn to rH cn o CO cn 00 CO to m 3 12 - ^ < OO i T C CM o OO rH rH to <3* © LO CM o LO CM rH o o cn oo 3 3 - CM * Cn LO LO cn O LO vO vO CM o cn o co CM O CM LO o 00 vO r—i tO LO CM i—1 00 O H r LO LO vO vO CM CM cn o co CO o O C o ctf 60b. NIV 30 2N 16W 212.40 - 0.664 0.131 26.40 73.60 L 0.358 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. without prohibited reproduction Further owner. copyright the of permission with Reproduced TABLE 1. Continued. q + <*3/^9PqH + qiH >[B3dqqgiaH pnj^ qusojcaj uoxqoas SOUBUaAOJLJ sSo sSo •osns pnw/pues dxqstmoj, quao.ia O O H t M C O vO o s O O M C H t H t vO H t to H t cn o H t M C cn 0 0 O C J ► O C O L t H t o t M C M C s s > O M C o o o o o H u n J • • • • « • • • • • • • • » • • • • • • • • • • • • • • • • • • • • • « • • H- O 3 - H t O T3 O 2 O v = 3 M C to o o o o o t H t O O C cn ^ C O O H o t H t O C H r o O L i— • . i \D H t O H t H t H t MO CM M C n c O L o O L ncn H t cn O V H r CO to M C M C M C 2 M C M > C M C O * H to O O *to t to H* to • • • • • : OvO vO O O O v H t n O C 0 0 i — t M C M C 2 o t M C * H —f t— H t H t O O O O o o o 00 cn M C M C H t o t o t o o t o t M C M C CO 00 03 3 - O o j - p < O v O L O L . > r o t M C M C o t 0 0 M C o O cn 00 o t 2 o t o !2 CO i • # O N O cn o O * H M C cn M C vo cn M C M C H t o o t M C H t vO o o o o t o H t o t O2 CO w M C CO H t 00 o o cd o t o t « • • - H H r - s r O L O L o t M C O L O C H" H* O C o t M C o o J • • • • • « • • • • • • & 00 o H t M C M C O O v M C o O v * H H" : 3 H t M C o o o O O vO H t O o M C M C O L cn O H t 2 o t • • • • • • « # # : vO ^ r O L O C O L H r t M C H r M C M C H* M C M C H t M C o o o O L O H t M C O C O L O L 3= O C H t O L O L H • • • • t H t cn 0 0 0 0 H t - H O v - H O o00 co o vO 2 W s 3 M C o 3= —itH t i t— H r H t o o o o o t O L o C^ CO H O O v M C D v O O O O C o t O L H t O L H t o t O O L M C M C H t o o H t H t O [>. CO H t H t o H r cn H t CO W M C O O o H t H t M C O C O O L O L O L o t 00 CO O L 00 O L O L 98 o tH o 00 o * tH t o CO oxq.Btf 0 3 t o cn LO vO LO o 0- t o o tH 03 t o t o cn pnw/puBs • •••••• t— i rH 03 03 tH o H" o SDUBUSAOJJ E CO CO co CO CO CO CO < < < CO aqoq X X X CO o cn vO rH LO c o t—1 O c n 03 vO cn O pn^ qusoasj • •• ••••• vO 0 3 03 tH t o t o CO 03 to t o t o H" o* tH LO 03 O rH H* cn LO 03 cn to rH O'* t o o LO t o LO puns ••• •••• quao-iaj to r-* c o vO vO tH O- vO LO vO o LO 03 CO H" c n cn o to vO 03 LO CO 03 c^. LO to H" tH tH cn to tH 03 to 03 to LO 03 pqH + »•••••• o O o o O OO O t—I t H t o H* o * H- o 0 3 qqSiSH 0 3 cn 0 0 LO t H 0 0 o * O o t H CO v o o * o - c n VOI/VZ •• ••••• t—! r H r H o o o o o sSo p _ o i X I I I I I I I *osns *Sb ^ O o o o o o o o rH o o o o o o (sureaS) •• • • • • • CO 0 3 o* oo r^. c n LO 3iin a 03 o o 0 3 o t o LO 03 0 3 0 3 0 3 0 3 0 3 0 3 0 3 2 : 3= sSlIB’JJ O O cn o o cn cn o rH r H tH tH T3 w 110x3095 p / i W w W 3= w W tH CO CO 2 : CO z CO CO m i-3 # # I PQ uoxqBqs c n o tH 0 3 t o L O o < a i duiB s o o * O * o* o* r*^ H Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 99 TABLE 2. Sieve Data. WEIGHT (GRAMS) Sta 18 35 60 120 230 Total tion Mesh Mesh Mesh Mesh Mesh Pan (T) 1 . 1.274 3.323 21.179 20.930 7.031 1.127 54.717 2 . 2.872 5.389 21.000 14.463 5.309 0.678 49.711 3a. 3.206 5.870 16.499 19.876 10.800 1.776 58.027 3b. 3.036 5.720 15.983 20.239 10.890 1.216 57.084 3c. 3.352 7.301 21.642 22.463 11.557 0.644 67.059 4. 3. 776 11.117 36.614 30.877 6.784 0.507 89.675 5. 0.864 3.193 14.545 12.550 4.145 0.231 35.528 6 . 12.778 33.047 39.955 11.240 1.471 0.181 98.672 7. 1.423 1.697 19.470 18.928 1.399 0.000 42.917 8 . 11.453 12.610 21.647 17.118 8.968 0.212 72.008 9. 1.102 9.294 37.572 28.022 6.836 0.333 81.159 1 0 . 0.246 0.932 5.671 13.072 28.541 2.526 50.988 11. 0.982 3.367 22.160 21.170 5.341 0.521 53.541 1 2. 0. 707 3.075 17.870 22.244 11.005 0.344 55.245 13. 7.161 16.425 39.112 19.888 3.109 0.137 86.032 14. 1.948 3.692 15.382 18.724 8.653 0.599 48.998 15a. 15b. 16a. 1.617 6.755 21.663 20.586 5.923 0.362 56.906 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 100 TABLE 2. Continued. WEIGHT (GRAMS) Sta 18 35 60 120 230 Total tion Mesh Mesh Mesh Mesh Mesh Pan (T) 16b. 4.373 11.637 38.256 27.487 7.553 0.190 89.496 17. 2.117 2.9 79 6.333 6.745 5.321 0.491 23.986 18a. 2.141 5.759 22.691 21.764 7.130 0.219 59.704 18b. ------ 19. 2.277 6.845 22.265 15.604 3.676 0.180 50.847 20. 1.313 5.409 23.727 20.171 7.003 0.110 57. 733 2 1 . 3.353 5.981 14.517 15.972 5. 790 0.256 45.869 22a. 0.796 2.494 10.336 12.335 5.107 0.183 31.251 22b. 1.098 2.959 21.952 28.235 9. 894 0.143 64.281 23. 1. 774 6.695 29.845 30.665 4.947 0.204 74.150 24a. 2.684 6.198 17.889 24.828 8.269 0.318 60.186 24b. 1.989 1.442 16.084 30.595 8.209 0.353 58.672 25. 4.961 8.992 27.191 33.892 8.713 0.246 83.996 26. 2.904 8.316 24.276 22.716 6.442 0.378 65.032 27. 4.128 11.441 25.262 22.461 6.486 0.204 69.982 28. 8 . 754 8.155 13.426 16.418 4.016 0.205 50.974 29. 1.520 2.089 11.340 21.315 7.281 0.266 43.811 30a. 12.510 25.403 46.136 16.782 2.503 0.326 103.660 30b. 3.400 8.961 18.624 10.534 5.773 0.260 47.552 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 101 TABLE 2. Continued. WEIGHT (GRAMS) S ta 18 35 60 120 230 Total tion Mesh Mesh Mesh Mesh Mesh Pan (T) 30c. 3.783 10.307 33.240 25.562 6 . 751 0.683 80.326 31a. 0.452 1.263 9.158 15.269 8.975 0.434 35.551 31b. 8.365 8.260 19.565 25.732 6.382 0.295 68.599 32a. 4.869 1.727 6.244 10.980 3.018 0.120 26.958 32b. 17.451 8.059 24.778 18.482 2.771 0.181 71.722 32c. 3.739 3.047 13.078 20.852 9.318 0.434 50.468 32d. 25.955 11.816 13.033 18.197 7. 719 0.621 77.341 33. 15.173 35.401 17.281 4.351 1.152 0.173 73.531 34. 9.130 16.643 56.940 15.699 1.100 0.171 99.683 35a. ------35b. ------ 36a. 8.708 11.768 23.344 19.650 5.409 0.341 69.220 36b. 12.162 12.233 14.265 10.532 2.397 0.167 51.756 37a. 6.720 17.323 40.553 7.882 1.081 0.125 73.684 37b. 7.547 22.882 56.493 7.427 0. 718 0.083 95.150 38. 1.801 5.124 18.834 16.608 6.547 0.207 49.121 39. 5.900 13.508 21.852 20.004 3.456 0.150 64.870 40. 3.759 12.644 21.950 8.231 0.449 0.092 47.125 41. 3.201 8.990 29.205 26.249 8.163 0.120 75.928 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 102 TABLE 2. Continued. WEIGHT (GRAMS) S ta 18 35 60 120 230 Total tion Mesh Mesh Mesh Mesh Mesh Pan (T) 42. 2.084 5.766 18.750 17.813 7.406 0.201 52.020 43a. 5.519 13.034 23.109 27.564 10.013 0.228 79.467 43b. 7.522 14.245 21.377 15.193 4.910 0.192 63.439 44a. 2.611 10.392 23.187 12.072 3.825 0.340 52.427 44b. - 44c. - 45. 1.659 4.884 17.882 10.092 3.121 0.269 37.907 46a. 2.338 12.332 30.663 17.576 4.445 0.298 67.652 46b. - 47a. 4.928 9.573 25.662 27.459 12.829 0.409 80.860 4 7b. 2.757 4.896 18.102 27.472 15.749 0.648 69.624 48. 2.210 6.803 32.817 24.784 5.815 0.597 73.026 49. 2.818 7.523 24.258 27.201 9.996 0.447 72.243 SO. 2.928 5.929 20.692 16.621 4.912 0.119 51.201 51. 2.393 8.991 25.075 17.768 5.564 0.153 59.944 52. 3.307 8.402 28.798 22.170 8.662 0.317 71.656 53. 4. 743 7.999 19.157 23.572 14.007 0.566 70.044 54. 5.453 11.632 30.112 31.389 9.813 0.196 88.595 55. 8.308 18.566 37.778 13.919 1.639 0.111 80.321 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 103 TABLE 2. Continued. WEIGHT (GRAMS) S ta 18 35 60 120 230 Total tion Mesh Mesh Mesh Mesh Mesh Pan (T) 56. 1.537 5.039 29.030 19.447 2.902 0.133 58.088 57. 8.976 20.030 30.011 14.974 1.276 0.058 75.325 58. 2.863 5.623 20.294 22.416 11.610 0.245 63.051 59. 8.791 19.471 18.829 14.658 4.311 0.3 76 66.436 60a. 2.853 5.084 21.861 23.214 11.078 0.211 64.301 60b. 1.644 2 .451 7.839 9.321 6.582 0.205 28.042 60c. 1.309 1.757 5.288 6.689 5.022 0.261 20.326 60d. 1.206 1.781 5.693 4. 804 7.688 0.362 21.534 61. 1.113 1.894 8.425 12.649 10.611 0.261 34.953 62a. 7.068 16.179 39.868 10.869 2.377 0.123 76.484 62b. 7.565 19.928 38.061 12.936 1.343 0.456 80.289 63. 4.106 11.934 39.611 25.250 5. 765 0.311 86.917 64a. 4.243 7.465 22.249 21.439 9.00 7 0.212 64.615 64b. 9.556 14.820 25.237 10.777 3.733 0.048 64.171 65. 5.525 12.504 26.514 9.109 1. 859 0.122 55.633 6 6 . 16.860 36.151 22.401 4.626 2.003 0.155 82.196 67. 2.356 10.560 55.292 19.621 2.321 0.311 90.461 VD 00 2.515 19.087 46.050 22.203 1.229 0.263 91.347 69. 2.916 6.744 20.843 22.765 14.790 0.011 68.069 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 104 TABLE 2. Continued. WEIGHT (GRAMS) >ta- 18 35 60 120 230 Total :ion Mesh Mesh Mesh Mesh Mesh Pan (T) 70. 12.251 24.852 18.049 8.368 1.306 0.301 65.127 71. 2.706 6.452 22.051 22.126 16.514 0.237 70.086 72. 4. 701 13.797 34.944 12.638 4.821 0.310 71.211 73. 8.016 19.667 29.807 5.394 0.736 0.048 63.668 74. 1.688 5.451 11.083 6.237 3.118 0.168 27.745 75. 7.915 19.353 54.697 11.374 1.808 0.375 95.522 76. 18.012 17.371 18.756 4. 719 1.470 0.112 60.440 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. without prohibited reproduction Further owner. copyright the of permission with Reproduced TABLE 3. Textural Data (B, bulk weight = total sand + mud; T, total sand weight) 0 x 001 0 x 001 x T 0 0 001 3q§T©M luooro^ 31[3t©m aqStOM auoorod 3uoox0d iqSiOM 3 xruw Xaboh sxnrouTw xauw Xaboh sxBaouiw (sui C x t[§i©M auooroj 001 09 qsow x 00T j b i u s sw 0£Z+0ZI qsow xisow 0£Z+0ZT 0£Z+0ZTqsoK sw 0£Z+0ZI qsow xisow 0£Z+0ZI sxo x ts tsw 09 trsow x sw S£+ qsow sw ££+81 qsow ) S ') iSt m ts S ii 3 M o x 3 q 3 3 3 UOI3B3S :).u . 1100 a U a oxdureg 0 0 OJO(j D.i a . 10(1 8 0 d T rH tH CM tH tH vO CO C-H >r « CM rH r-H o HC vO c CM VO tH CO LO MCD CM O tH C-H <3* to H t o CM CM vO o CD o 0 0 CM CM CD CO O CM - h • • » « ♦ • • • • • • • • • • • • • • • • • • • • • • • • • • • « ♦ • • * • • • • • • • • • • • • • • • • CM to CM H* O H t VO c CM o CD to CD c H" c CD CD CO O CD 1—i c DtH CD ^ r O t-H * H LO O CM - - - - h h h h • CO O tH vO OL O<*H* <3* LO LO LO CM n r H" tH rH CM CM 00 C-H r-H O L 00 H* o o o o t o t ^ r LO CM CM CM MC CM CM CM to c CM ^ r CO ^ h • • » • • • • * • • • • • • • • • X* DCM CD HH* tH LO H t O v o t tH c OLO CO DLO CD t c H* CM rH to CM CD t-H O LO to C-H CD I>H to CO oto t to to H - - h h • . o tH r-H tH O H t to vO o t CD tH to CM H t T—i H - C r-H to CM o r-H O r-H LO ^ r o LO HO rH o CD CD O OvO vO o o o • • tH - H HvO tH t-H O CD *CD H* CD 00 r-H tH O CD o o t CO CM H t 00 MC CD CD CM H t ^ r CM t-n o t o to rH LO rH o o t-H CO C-H OtHtH t H t LO t H • CM tH t VO CD CD r-H CD *3* CD o t a CD OO Ht CM tH tH tH CD rH O L o CM OCO LO LO o t H * • • • vo Hto tH O o t <3* H t OCM vO CM H r CM vO CM 00 *CM H* O v CO 00 CO to t-H o O L tH LO • • 2 1 t vO r-H O VO rH LO LO CM t-H H" t-H o t CM o O o O tH LO O CD o t o CM O H . 105 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. without prohibited reproduction Further owner. copyright the of permission with Reproduced TABLE 3. Continued. 0 x 001 0 x 001 00 0 x 001 rjqSiaM qiM rj.uaa.iaa iqgiaM aqSiOM Auaojaa rj.uaa.iaaaqgiOM qiM rj.uaa.iaaaqgiaM rjqSiaM rj.uaa.iaa siBJauxw siBJauxw x T iauw XAtan siaaauiw ( ( suiba suiba 001 001 qsaw 0£Z+0ZT qssw 0£Z+0ZI qsaw xisaw 0£Z + 0ZI 0£Z+0ZTqsaw qs 09 qssw X qa 09 qsaw X sw S£+ qssw sf S£+ qsaft S) S) ^qSiajvi iqSiaM uoTrjBis rj.uaa.iaa 3 0 -uaa.iaa axduies g £Z+ g X ab g 0 8 9 ZI 8 h T T vO rH o o t co CM rH O rH O v 00 CM vD vo rH rH o v CM O O o t o o LO CM CM OO rH to o CM LO rH OO to o CO to CM • • • • • • » • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • « • • • • • • • • • • • • • • • • 1 0 t o \ vO o rH rH o CM o LO rH Ci rH *3* CM i C to 00 LO CO O CM o LO C*^ -H 1 8 VO O v CM co t t CM O v r-^ rv. CM rH O O rH o CO to oo O HvO rH oo o i C CM CO rH rH rH o t o o CM oo -H -H • Oi t o t MCi C CM rH t rH rH 00 to t to *3* rH *3" o t *3“ i C MrH CM i C HCM rH CM LO rH rH OLO O v LO MrH CM LO LO -H -H -H -H 1 0 « O Ht-H rH 00 HrH rH rfr co LO CM VO 00 o t CO OO 00 o t oCM to CM o Ci o o i C to CO to -H • vO rH O v t to CM Ci Ci oo o t CO CM o t CM o t * 00 C*^ t LO rH <3* CM t OO LO LO CO 00 -H -H -H 1 9 • • t-H VO i C o t vO O v t t-H CM oo vO t CM O CM r-** r**. CM i C CO rH o t to vo LO to LO LO -H -H LO CS 15b. 106 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. without prohibited reproduction Further owner. copyright the of permission with Reproduced TABLE 3. Continued. 001 001 001 001 q9 0£Z+0ZT qs9W X q9 0£Z+0ZI qs9W X i § q . q i S q i t T § q i xuuw Xab9h sx^uguiw )lSt t).l{S tj.u93.i8d iqSiaM aut§i9M tj.U90.i9d SX'BA9UI^I XAB9H (SUIBUS) aqST9M ( qs S£+ qssM X tsw S£+ tjsow x siubj 0 : qsgp\[001: 09 x 001 t{S9H 0£Z+0ZT sw 0£Z+0ZI qsgw sW 0£Z+0ZIqs9W HS9W 09 x 9 3 9 9 tj.U M tj.U M S) tJ.U M tJ.U M UOTtJBtJ-S tJ.U 9XduiBS 3 9 3 9 3 9 3 9 3 9 I . i . i . I . I . 9 9 9 8 9 9 8 d d d d d I T t—1 o H t H t H t vO ^ r to tH tH o to LO to tH * H t vD O v o cn " H O CM cn CM * H vO CO to O LO o t co OOO CM O LO r-v o 3 cd • • • • • • • • • • “ • • • • • • • • • • « • • • • > Mcn CM r>* tH 0to 00 tH rH O * H t LO vO CM H* o 00 LO O r " H o cn o Cn LO O D v LO O V LO O v O CM o t H t to o 00 H • • • • • • • • • • • • > MO CM to CM * H CM O Cn LO H t O to to LO o O v D v CM LO LO H t cn CO LO CO CM H t CM o o • • • • • • • • • • • Ht tH tH tH vO - H * H O0 rH 00 tH CO rH H t H t to C7> cn H t to tH CO 00 O O tH o Ot o tH LO 0 0 0 0 cn * H cn cn H t to o 0 0 to to to H t H t 00 H t CM 00 cd • • • • •O 00 • t • 1 • I l • i v H- vo i i 1 1 tH CM LO tH to CM o H* D v o C^s cn H t oo H t cn cn o c to 0 0 » r^ o o o o « • • o CO tO - H vo tH CO CM CM CO LO to tO t D v CM H" " H D v o o H- vO o cn tH MCM CM o CM ^ r CM O L - r O D v ! — • • • • • • • • • • • • • • • • « r*^ Cn < MtH CM o H t O o t tH H* D v LO H t H t CM H t ^ r o to O to CM cn cn - H CO CM o H t 3 • • * tH tH VO tH t-H o * 1 ^ LO CM C*"** oo CM H t oo H t oo CM o t r-> CM O L 00 O L LO o cd • • 107 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. without prohibited reproduction Further owner. copyright the of permission with Reproduced TABLE 3. Continued. 00 0 x 001 x T 001 0 x 00T q.q§i9M luaoxad q.uaoj;ad iqStaM sxBJiauiw SXBAaUT^ XAB9H xqSxaM xuao-iad qiM TU30-tSdaqSiaM ausoxa^. ^qSiSM SIA) XI{8 (SUIBAS) SI.§ lf 9J\l l9 llfS (SUIB.I§j x 001 U qo 09 qsoH - UUL x 001 sw 0£Z+0Zt qssw sj 0£Z qsajj + 0ZT 0£Z qsaw + 0ZT sf 0£Z+0ZTqsaft 0£Z+0ZTqsaw ^ qsow S£+8T uoiq.BXS XXI90 JL9J sw 09 qsaw aiduiBS g g X ab g t 9M 9 h © CM M C o o —f T— © t H r o t M C O H r H r CM n c © o O L n c o t H r n c "*cn c C"** M C H r t © cn CO 0 0 n c O L M C o t © O L n c t o t M to C O L -H H - H - H - • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • » • • • • • • • • • • • • • • • • • • • • • • • • • • • • © V H r o t M C M C H r n c 0 0 H r t “ 3 * H r O L t O “ 3 * CM o t LO t o t O O L «Sl" n c o H r o t H - -H H - • • • • • • • n c H r O v n M C c 1 T— “ 3 * cn CM o t o t o n c © CO O L 0 0 n c M C o H r M C O L oto to o t © v -* C o o t o cn o d c • • CM © H r n c © H r o t O © M C © H r © 0 0 00 *3* 0 0 O H r CM H r n c m c o O L o t O t O C T“ H o o T—i M C H r M C t H r o c CM © v LO 0 0 H r M C O L o t O L M C t to o o oCO to O O o t CM O L LO © H - H - • • 0 0 H r H r n c n c t O L O L oo CM © CM CM cn —i T— H r LO n c CO LO o t n c to o t O L O L 0r- r 00 o t O L O L H - * • • • • • © o t 3 0 O o t i T— —ioLO L o i T— 0 0 © © V o H r m c n c 3 0 O L O L 0 0 5 0 o t H r t M C M C o t CM . ^ r o t o O L -H © cn MCM CM o H r © O L O C o n c n c o t o t t o t to O C CM CO © v o t o o H - . • • o o c oo O v © oo H - r CM CO O L © M C i T— O O C O C O L O L cn © o o t cn H r o CM O L o t • • 108 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. without prohibited reproduction Further owner. copyright the of permission with Reproduced TABLE 3. Continued. 0 x 001 00 x T 001 001 S X B J : 9 U t J iXA \ [ B 9 J J S X B J 9 U T MXA [ B 9 H 3.q§i9M q.U9DJ9cJ qiM TUSOJSd iq§i9M ( 11 (SUIBAS) uiM q.u9oa9£ lu§i9M suibjc x x 0 x 001 0 x 9 x 001 {S SK 0£Z+0ZI^S9K *IS9W 0£Z+0ZI i{S9W 0£Z+0ZI sw 0£Z+0ZIqsgw sK 0£Z+0ZTqs9K t ------9 sn S£+ qsan Tjsaw $£+ ) S m lugo-ig^ . 9M i9 § x.q uotiBq.s augo-ig^ sH 09 qs9H i[S9W 09 q.usoJSd 9xduiBS 9 5 ------8 8 T T H r t O v M C cn © LO © cn i — T O C i T— cn M C O C O L ^ c t * 3 * O O —i T— O v O O L CO o O L O O © CO © O O L 0 0 H H C c • • • • • • • • • • • • • « * • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • 2 1 17 O v I X O M C M C 0 0 © CM cn CM CM O C M C O C H r O v O O O v co M C M C M C cn co cn H r LO CO to o o O C O C no cn co « c o © O v » > F M C M C i T— n c O M C M C —i T— " 3 * i — T 0 0 oo O CO o t © O C O C O o co o • 1 4 0 0 © rH © o v H t M C M C i T— O v nO cn i T— co O v O O M C t © o t O C o LO M C M C O L o —iT i T— CO i T— O L M C —1 H f t c • © X " 3 * O O —i T— vD M C cn cn © —i T— © . ^ c cn O v O C i T— O L CO CO CM r*^ 0 0 LO —i T— M C OC CO CO CO • • o M C - 3 * O C O L M C H r C r O v i T— O L cn M C i — r O v CO CM co O C to cn CM O C M C H r O C cn cn O C O C O L M C O L O H r M C O C M C O L O C o O O C H r d c • • • X “ 3 * i — t M C o o rH CO “i T“ “ 3 * © OO 3” *3 MCM CM O L O C cn M C cn cn O C O v O C O L o cn LO • • • • • • • • • • • • 1 2 13 t * 3 * © O L O C CO T—i O C CO —i T— o O H r © cn i T— cn i T— CO t LO o o H H CJ • • * • • • • • • oo © x • O L o O L LO M C O L i O H r oo o c i T— o O O O L CM —i T— cn i T— O v CO CO CM co o co co O L • • • • • • 18 109 110 * 3 * t o LO to C n a 0 0 LO C M C n C T i 001 X qssM S£+8 T • • 1 ( • ••• L O r H O r H aqSrsjn iu sd jsj C M r H r H r H r H r H CM to 00 vO r H • 001 x O o O 00 O 8 qssK S£+ T vO o CM CM H{Sx9M ausojs^ vO CM to to to to LO v O cn a 0 0 0 0 v O c o 001 x qsaw 09 • • 1 i * ••• 0 0 C O r H 0 0 Cn E ^ CM r H r H CM O C M C M o to o 001 x ------LO r H LO o qssK 09 • • t 1 • • • • to to LO Cn 3.i[§t9M ^uaDjaj CM LO to CM LOLO a r H r H CMCM r H 001 x 0 0 LO L O c n t o O qssw 0£Z+0ZT • • I I • • •• CM 0 0 CM " 3 - ■<3- at{§tQM auao-iaa r H 0 0 L O O 0 0 o O ooi x 0 0 CM cn r H LO US3W 0£Z+0ZT •• 1 I • • • • vO O ^d" CM o o q.q§T3M mso-isd r H t o CM r H to LO Oi O o qS9H 0£Z+0ZT to o o o o CM vO SXBJ!9Xirp\[ XAB9H o CO ( 1 C M r H O t o • • • • • • aU90J9d LO to ^ 3 " to LO Oi CM O qsaw 0£Z+0ZT L O r H o t o SXBJ19UIK XAB9H CM v O 1 1 o t o T3 • • • • • • 0 (suiBaS) x^^T9M o o r H O o o 3 3 •H •P C to CTi C n c n t o LO o O C n LOCM o cj qsaw 0£Z+0ZT LO r * ^ o cn cn r H •• 1 1 •• • • (SUIBjg) aq?I9Jl| LO o LOCM 0 0 O O r H 23.155 0.467 2.017 47.13 11.56 38.34 9.40 14.53 3.45 to r H C M w PQ UOTX.BX-S t o cci rO cd r O cd p O oo < axdui^s to to LO LO v O v£> t o H t o to CO to t o t o Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. without prohibited reproduction Further owner. copyright the of permission with Reproduced TABLE 3. Continued. 0 x 001 0 x 001 001 00 qiM auaoxaj iqSiSM aqStOM ^uao-isa §9 lUSOJlS^ m§I9M S X B A S U T J f lXA J B 3 H auaoaoj iqSxsM sxBaauip^ aqSiOM iuodjioj ( tuoojis^ iqgtSM x T SIAj I§T3M T § tI a (SUIBA§j x a b i u s 001 001 sw 02Z+0ZTqsew sw 02Z+0ZI qsaw sw 02Z+0ZTqsaw 02Z+0ZIqssW usow qa 09 qsaw X X . t { S 8 WS£ + S T iisaft S£+8T ) S M s x S q i uox^Bis lueoasj sw 09 qsaw 02 aiduiBg a S X Z+ absh 9 0 ZI © t o © © © J C o t J C © o t © © © tH © o o o t © © CJ CJ CJ CJ CJ JH © H* CJ CJ tH to © tH © 44b. ll I Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. without prohibited reproduction Further owner. copyright the of permission with Reproduced TABLE 3. Continued. 001 001 001 0 x 001 x * uxM auaoxaj lugxsM siBxaux^ siBxaux^ SXBXSUX^ XAB3H q.qSx9M xusoxaj xqSxsjvi xusoxsj ( auao-ia^ aqSxs^ SI-S ^[X9M ^l[8X (SUIB-tSj q.uaoxaaaitSiSM x suibx 001 001 SW 023+031^S3W ^S9W 023+031 sw 023+031 qsaw 023 tfsaft+ 031 qa 09 qsaw X qs 09 qssM X sw S qsaw S2+8T qssw S) xq§x9M UOXlBq-S q-uaoxacj 023+031 q.uaoaacj aiduiBg a a ^C absh a 2 + 8 T M C “ 3 ^ D v t i C M C H r O V M C 0 0 LO LO 0 0 LO M C H r *^ C i C T—i H r M C * 3 < o t i C O o t H r o t M C “ 3 * v - r 0 0 to O t M C o O H r O L H • • • • • • • • • • • • • • • • *5t 5 •* H r O C M C M C O v O o t M C o i C H r to o to r—i - r H r O L o t o M C O L H r M C “ 3 * O v o M C M C O aJ • • O v • t • t 00 I • t i • 1 • 1 LO L 1 t O V i C i C M C M C O to to H r fr sf * H r O l C CM to M C i C H r O L i C to to H r H r 00 M C o M C 00 o t ctj • • • • • ♦ H r M C i C O v O L H r n c i C i C M C l C O 0 0 O L t 0 0 O L O L to 0 0 H r M C o i C H r J3 o M C ^ * r o t H r o i C o t M C H • • • • • • • • • • • • • • • • • • • • • • • • • • • l C H r - 1 ^ H r H r i C H r O H r O L O v M C M C o t o t O v H r O L o t to oo o o O C O L 00 • • • • • • • • • • • • • • • • O L * 3 < O L d’ 'd H r M C O L O L CNJ 0 0 O L M C o M C i C OCO M C LO to c^. H r i C to O L i C l C H r O v H r H r H r o t r^. H r O L i C r*** H r H r H r O L 0 0 o t o O L O L H r H r H r * 3 < O O L O v i C i C O v CM LO O v o O v 0 0 CM o M C H t O C to o M C O C to O L O O L O L . . O L CNJ M C i C M C M C H r H r M C O C l C O to o t H r H r ^ r O i C to o t O C 112 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. without prohibited reproduction Further owner. copyright the of permission with Reproduced TABLE 3. Continued. 001 02Z+0ZT qsaw * 001 U qs 52+8T qssW ------UUL x 001 S2+8T qsaw X00T qa 02Z+0ZT qsaw X J ( 3 X 0 9 U 1 M 3 T § [ 1 1 [tM aoxaj m H[8t9M aq§TSM 11190^8(1 3.qSi3M augoja^ qiM mao-ia^ iqSiaM q.il§T9M TuaoJOcj SXBX3UIH XAB9H xxu^ Xab9h sxBxaux^ six) i'q§X (suiexS) iqST (surexS) 001 00 g sw 02Z+0ZTqsaw sK 02Z+0ZI qs9K ^S3W 02Z+0ZI x s^ 09 qss^i x T qa 09 qsaw x uotibis J 9 X 0 9 U 1 aiduies g 9 9 M jvi oo CM O CM t *3“ O v O L CM to o t o o t CM CM o 00 o t o 00 o rH oo cn rH o t O L o t rH rH 0 0 o LO LO ^ r o \ o H • • • • « • • • • • • « • • • • • • • • • • • • • • • • O v D v Ho tH LO o LO rH CO CM CM t n c LO O o CM LO to LO c^. cn vO LO to CM OO 00 to CO H • • • • • • • • • » • • • • • o v o CM rH *Ocn O H* to to cn rH n c CM rH MLO CM O o cn o l C 00 H r LO 00 G1 o i T— LO CM t O > o t !>. H • • • • • • • • • • • O v o o v CM H t O L O v H r cn o t oo o cn o - r to CM t o o t o t ■'tf* t rH Cn OLO LO LO LO 00 LO CM o rH LO C^» H H • • • • • • • • • • • • • • • • h o O 0 0 r-*. H t o r*-. ncn cn r-N O CM rH T— t LO T— O v CM O v o o t O t to to nO cn CM o H « • * ( t ^ r ^ r vO h O v rH i C Hto t rH O CM CM O L H" CO CM LO CM tH LO 00 00 to 00 t O rH o t LO 0 0 LO rH rH OLO L LO O L MC Mvo v CM CM CM o t o H H • • • • • • • • • • * 0 0 CM cn H* cn O OLO L LO o t ncn c cn rH o tH o cn LO o o o t o Ocn rH CO cn CM 00 to to LO cn O v o t to 00 • • • • • • cn O v O v H t CO CO MvO v CM LO o t O L LO CO CM O C o t CO CM LO CM LO vo o vo to • t VO H* H" D v cn O L to to CM O v o cn t o cn to o t O L o t O L CO CO CM LO to o t H H 03 • 113 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. without prohibited reproduction Further owner. copyright the of permission with Reproduced TABLE 3. Continued 001 0 x 001 0 x 00T 001 x qiM auaojiod aqSiaM qlM lUSDJiSdiqSlSM aqSxsjvi qiji AtisoAO^iqSiajvi sxeaautw sxeaautw xjai Xabsh sx^jiauiw ( ( ^ 001 001 ui a ib su ui a ib su qssw qssw sw 02Z+0ZI qsaw sw 02Z+0ZI qsaw la 02Z+0ZTilsaw qssw qssw qs 09 qssw x qs 09 qssw X ) S ) S t§T9M 9 T lt[§ M i8 S q.q 0£Z+0ZI A UOIABAS 02 a a usdabj axduiBs A Z+ a absh 0 ZI VO i O H* CM i C tH HtH rH VO ) X LO to LO to O v O v r-** c^. 00 tH i O o o t LO H* CTi rH o v T-i t—i t—! LO t—1 tH LO LO © © LO to CTi O O tH CM LO LO LO • • * • • • • • « • • • • • • • • • • • • • • • • • • • • * • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • • o \ o O CM O v tH t OO tH r*^ MC MLO CM CM CM tH to VO LO LO H r CM i O ^ r O) O v O v t tH CM H r CM rH — O H • • i O O v vO o t H- o CM tO I T— tH LO r-H *0 o t LO CM CM CTi to LO O H* CO C^ CM CM CTi 00 O v CO tH O o • • • • • • • • CM O v rH t H* rH O'. to rH o CTi O v to to O v O v o vO 0 0 VO vO CM O o to CM oto to o rH H • • • • • i O tH CM rH o v o o LO CM * H * H rH LO * H to O rH OvOvO v O v vO CM CM to o CM H o 03 - H o v t 0 0 to to to O C CM 0CO 00 A - H CM o O v rH O v CO ^ r tH CNJ CM ^ r CTi CO o O v tH o CO H 3 . . . 13 o v —! T— OH o t H" LO rH OO T—i OO LO O v rH r—j tH tH h LO LO LO i O O L CM CM o t O v O O L CM to O o CTi tH LO o t to o * o * H o HtH rH rH CM o Ocn LO CT> H r CO to oo to H* O v to tH O tH o t rt cn i I H* . cn tH . ^ c o OO i O CM o o t O 3 A " H O LO O v rH o t O to ^. C 0 0 CM LO CM o • 10 114 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. without prohibited reproduction Further owner. copyright the of permission with Reproduced TABLE 3. Continued. 0 x 001 0 x 001 001 001 q.q§i9M iuaoxa^ AqSxajvi AU90A9. l C o o o o CO co • • • • " H H t H t O O v l C H t " H o H t 0 0 VO O LO LO H t CM CO CO o CO O l C O CM O v o * H - H O v O v o c CM LO CM T— 1 0 0 l C S E ^ r H t o o ^ c-~ r^» MfO CM H t l C l C CM MCM CM O v O l C CO '- - r LO • —1 t— l C o CM O l C H t l C CM O CO H t H t CO H t CO O v H t O v o t O H t LO O v • . 5 1 1 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. without prohibited reproduction Further owner. copyright the of permission with Reproduced TABLE 3. Continued. 001 001 00 00 * * 3q§T9M 31193.193 3q§T9M 3U33j;9j q.i|Si 3q§T9M 3U93JC x T 3q§T9M 3U93J93 3q§X3M 3U93A93 x T X.9Tt / H 9 B /A SXB.I9UTft[ xju^ /AB9H sxtjgut^ ( ( 1 0 0 001 ui a ib su a siub sW 0£Z+0ZTqs9W 0£Z+0ZI qs9H sH 0£Z+0ZI qs9H 0£Z+0ZI qs9K qS9W 0£Z+0ZT qg 09 qsgw x ■ * sw S£+ qsaw S£+ qsaK 8 M ) S ) S 3qSi9]vi M 9 T § q 3 1 31193.193 UOT3B3S 3 9 J 3 9 U 3 {S a a 9XduiBS 0 09 H I a 8 8 3 9 T T t 0 to to MO CM cn * *3 O CM r-i Oi CO LO rH rH rH CO CTi CO LO to OLO to LO tO OC O CM LO O CO H • » • • • « • » • • • • • • • • • o v o v CM rH \D cn 0 MLO CM CM CM CM CO rH r-i V0 rH CO * LO LO LO r*^ 00 rH CO to cn 0 LO co 0 3 » • “ rH o v O v O V CM cn O v rH rH CO CM O LO 0 rH CO to CO to i - r O v to rs'* vO rH O to CO to cn to • • APPENDIX II 117 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. STATISTICS A statistical study of textural and mineralogical data from surface exposures is presented herein. Analysis was accomplished using the statistical package program (STAT PACK V4) and the PDP 10 time sharing computer in Western Michigan University's Computer Center. The stat pack program is an integrated statistical package written for terminal use. Among the statistical operations cal culated and presented within this appendix are the fol lowing: mean, standard deviation, variance, median, mode, range, standard error of mean, co efficien t of skewness, coefficient of variance, z-score, histogram, Chi Square, T Test, and Mann-Whitney U Test. A complete discussion of the above statistical techniques may be obtained by consulting Folk (1968), Krumbein and Graybill (1965), Spence, et al., (1968), and Mendenhall (1975). All surface data presented in the text was examined with Chi Square, T, and Mann-Whitney U Tests. The Chi Square Test tests population distributions as a whole (Krumbein and G raybill, 1965) and is used herein as a test of normality of population distribution. The T Test exa mines the significance of difference between two means, while the Mann-Whitney U Test s t a ti s t i c a ll y te sts the independence of data and indicates whether two independent 118 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 119 samples are from the same population. The Null Hypothesis associated with each test follows. Chi Square: The distribution of each popu lation is not normal. T Test: The means of each population are equal. Mann-Whitney U Test: Two independent sam ples are from the same population. Critical values for the Chi Square and T Tests may be obtained by consulting Mendenhall (19 75) Appendix II, Tables 4 and 5. The Mann-Whitney U Test re je c ts the Null Hypothesis if [z|£2.5 at the 0.01 level of significance, 1.96 at the 0.05 level of significance, and 1.64 at the 0.10 level of significance. Using the T Test and Mann-Whitney U Test, both between lobe and w ithin lobe analysis were performed. Each lobe was divided into east and west halves and designated as follow s: LM, Lake Michigan lobe 1, Eastern half 2, Western half S, Saginaw lobe 3, Eastern half 4, Western half Table 5 records the sample stations associated with each half lobe designation. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. TABLE 5. Sample statio n s associated with each half lobe designation. h a lf lobe Sample Station designation 16, 17 33, 35 43, 44 45, 66 10 13, 14 29, 31 32 64, 65 54 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. without prohibited reproduction Further owner. copyright the of permission with Reproduced TABLE 6 . S ta tistic a l data from sand/mud ratio, percent heavy minerals in the fine + very fine (120+230 mesh) sands, magnetic su sc e p tib ility , X-ray d iffra c tio n , and garnet/epidote+hornblende ratio analyses indicating the lobe designa cd • H ■ • i to Cd , tion (lobes: LM, Lake Michigan> lobe; S, Saginaw lobe), number of observa- ' / / H • d n > T3 H • H • 3 T '—' .o S / C/3 a (D H ■ O +> +-> P p ■ __ __ ------^ro r^ c > cd O 5 C S 0 fH 0 dfi f cd © © > o > 3 c/3 T3 C C •— cd t/i co to P co cd cd 0 O T3 h • • A • N N > ' e N V v— —' v— /—N / t r * 3 T CM H • H • S -H p --- U £ C 0 0 X O £ s s r* --- A 0 cd cd £ £ € cd X © 0 £ MH 3 ^ s s X s cd 03 cd c O « • • HI ' > N / A! (/) /■ CM H • H • r ■H u O o CO W T3 S S > 4-> P — \ — — £ E > c O £ o 0 £ 0 0 cd +J 0 2 C 0 O U O cd U r— 0 O £ • CO 0 m LO cd O h • . - • < ' \ \ *h E v) 0 0 X saqoq ubow •sqo apow •PTS •Aaa • •paw *A*D • XBW •uxw jba N3S XS H • H • CO LO H r P s 2 OvO v CO l f Lt cd dcn O cd £ >N CO cd Cd * O v H r * d ^ H r CM O v O L o \ i O CO H r «d* CM o H H r r H r -•d* O O o v o t o t O O H r H r o o t 0 0 o t o t o - d < H r cn CM H r H r o * d ^ C-*» O O LO o t n c CO to o o - d * cn o t + * • • • • • • • • • • • • • * O H r O O L n c n c 0 V O cn *d- H r rH r * d ^ O H r " d * i C n c o CM H H r r H r CM - d * i O * d * CM o H r r-% ncn CM CM CM CM to co S • • • • • • • • • • * CM O H r *d* o o t H r H r " d * H r 0 0 CM H r O L cn oo O v oo CM o o o t CM C v o t n c o n c o m c o l oo r OO VO •rH O L to o • • • d o H • CM O CM H r H r CM O LS CL to •P + D < tf) 'SI c * - r 0 e g o o cd c 0 C LM+S 55 3.190 1.448 2.098 2.840 2.700 8.400 0.120 0..195 1.774 45.406 LM 37 3.218 1.372 1.882 2.840 2.700 8.400 1.720 0.225 2.319 42.633 S 18 3.131 1.634 2.672 2.850 0.120* 7.800 0.120 0.385 1.080 52.200 121 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. without prohibited reproduction Further owner. copyright the of permission with Reproduced TABLE 6 . Continued. saqoq apo^f *sqo •Aaa ’JCBA •PTS •paw • *A'0 W3S utw *HS m •pH X +J X fH B c p CO o o e I •K -K -K O v o -5 3 - - 3 -5 o v O o o o 5 0 O L o v o o o O L M C M C O oo M C p - t ■53- tO O V O v o o Lf) *3- 5 0 H H O C - CM t-p o o o o N - c O V o o O 00 vO 05 o o o H M C o t o l o r o i r H o o o o « - o r p - r o v p - r 5 LO 0 ^ - t ■53- o o O V O C p - c O t H H ! i— i—I o r-i o o O V o O L O L 5 LC O * 3O - " 3 - r - »O O O O O O H o o o o t 5 O V 0 O V O 5 0 o o o o o <3- LO 00 o t | — i O t O C S + • • • • • • 53 05 05 t — - CM M C i 53 - p 'O H t • rH CJ3 -p p • P - + u 0 0 0 c & o 0 o e Q 0 p US p ca o - O 7 I 7— O t- S " S pJ S O L l O - ^ ■ M H H I — i O L I — l CM O O 'S- o ^ o o o i—tt o i—I 5- CM o t ■51- M C 5 0 O t 0 0 5 0 5 0 O C ~~- M C f 5 - ~ t~ O O O o o o O L o t O L o o o <3- LC| /5 t o o o O o t O 5 O v 0 O L 0 0 0 0 0 O 0 v I i— M O t H O t CM CO vO O CM - l i O O O O O iH CM OWN H O o o o 1 CM CM O o o o O t I i— M C 5 O 0 O O M C o o o O L O L O L o o o + SCO I — -IOO -IOO • • • v r 5 0 O v O L * 3 * * G) i - r i - r Chi Square Analysis Sand/mud ra tio analysis X2 = 0.000 with 73 df and probability of 1.000 Percent heavy minerals in 120+230 mesh sands X2 = 0.000 with 73 df and probability of 1.000 Magnetic susceptibility X2 = 6.472 with 48 df and probability of 1.000 X-ray diffraction LM+S X2 = 4.285 with 64 df and a probability of 1.000 LM X2 = 1.666 with 21 df and a probability of 1.000 S X2 = 1.826 with 43 df and a probability of 1.000 Garnet/epidote+hornblende LM+S X2 = 10.729 with 56 df and a probability of LM X2 = 7.632 with 36 df and a probability of SX2 = 3.120 with 18 df and a probability of 123 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. without prohibited reproduction Further owner. copyright the of permission with Reproduced TABLE 7. Mann-Whitney U Test for sand/mud ratio data and for percent heavy m inerals in 120+230 mesh sands. •H OO ■P C £ 3 CO t f OS O ►a t - r • > X T3 H • rH rH OO s ! S I 2 Q +J CD > > o > c CO f-i 0 > cn cO cu cO cfl fH cO CSl J S C : —I O r M C M C i - r H r I *— cm —( T— © o o i T C M C t M C i ~ r M C O L o o o H r © o o l o M C © o o O t O L o o o H r H r H r O t © © © © © © © o c c 0 0 — i • * • • • • • « • • • • • • • • ♦ • • « • • • • • • • • « • i © *3- 3 •* © H r M C M C M C M C M C © © © M C M C © ^> C M C o © o M C © o © H r M C H r o n t © © © © © © © O O o c o o ^ M C H r © H r © H r © M C H r © © O O H r H r O L H r © o © © © © © © © o t o t o t © • © © o t © © © H r M C © M C O L M C © © © © © © © © © o t M C O C © © © © © o © M C H r H r H r • • • • H r M C ■*3* M C O L © x r o t H r H r 0 0 o c © o t o o © © O L H r o t © - co o t H r M C 0 0 o t O L © © © O L H r 3 1 - oo- M C O C XI © M C © O L © © © © © O L © M C M C O L H r a, x) x: K> •H CM o CM o •H i—i 4 + cn 0 5 S > 0 c £ o cn CO cn 0 c 0 cO > s c cO cn u X -> h x © O C s 2 H r H * x Q © i—i •rH CM -> 4 0 > 0 C > cC 0 X 0 cn > cO > cO fi c0 c0 H r M C H r M C • • * 3 * H r M C H r M C © to O C © © © 0 0 © O L M C © to o © H r H r O C 0 0 M C © © © © © © © © © O L H r M C ^ r ! 2 O f M C M C H r H r H r M C M C o t M C CM *= CO 1 • • • ♦ • • • • • • • • • • • • ^ r © H r H r H r H r M C © M C © M C H r H r H r © © H r © H r H r © © © © © © © © © © © © O L * 3 < M C H r H r M C © O L © H r • • • • • © © © o o © © © © © © © © o © o t © © M C o t M C H r to o t 3 • • • • « • • « • • - CO -vf -vf CO- H r © M C H r 0 0 © © o to to M C © © © H r H r M C M C H r M C M C O L o t 0 0 o t H r H r H r © © H r 1^ O O C C O L © O C © © © H r to © © © to © © © O L M C © • • • M C O C H r © © © © © © H r 0 0 * 3 * © H r t © H r H r © M C © H r X3 © oo © - 3 * © © © M C © O L © 00 124 Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. without prohibited reproduction Further owner. copyright the of permission with Reproduced TABLE 8 . Mann-Whitney U Test for magnetic susceptibility data and for X-ray d if f ra c tion data. O r •rH •H •rH •rH S P P p o 3 P P H • H r H • H r Q o c P « > (D > O c u cO CO > CO P d c < n c n c H r 0 > 3 S 0 CO M C d H r M C • H r —j r O v H r t H r M C o t H r 0 0 H r o H r H r H r M C n c o n c o o O o o o o o O o o O o t o o O o O L O L O L o O L o o O v i O o n c o t 0 0 o t -H • • • • • • • • * • • • • • • • • • • • • • H r H r H r M C H r H r M C O L 0 0 n c o t o o o O L O L O L O L o o t O L o t 1 - r • • • o v H r o O “ 3 * H r 0 0 O L o t 0 0 M C O O O VO O L CO o o O o o M C 0 0 1 o t H r H r M C VO o o O O v H r H r n c n c o O H r o o o 0 0 o t o t O L H r M C o t • • • • H r H r H r O v H r O L O o o o O L o o M C o O H r O H r 0 0 O L 0 0 o t o t O o t M C • • H r H r 0 0 o o H r o t o o O o O O M C H r o o o o o O M C H r O O L O L 0 0 O L • • o t N p s O C H r o t o v o O O L O L n c o t o o o t o o t o t 1 • •rH Doo 3 o t o l o l 3 . N [ o t o O L ^ * C H r H r o o o o o M C H r M C o o c o t H r M C 0 0 0 0 O L O L O L o • • • • • • • • o n c n c O M C M C O L O L M C o o O v 0 0 P O o 0 0 o o O L n c 125 <4H •H H r • H r • o LO p p > 0 0 CO DO e o S3 significant at 0.01 level; ** cO CO Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. without prohibited reproduction Further owner. copyright the of permission with Reproduced TABLE 9. Mann-Whitney U Test for garnet/epidote+hornblende data. X> rH JD •H •H 2 CO o s CM -P significant at 0.01 level 126 127 - - S S 1. 327 1. 0.000 0.000 1.634 ------LM LM 1.634* 0.000 1.327* 0.000 — --- — — M 3 3 4 -- 3 3 4 0.000 0.000 0.560 0.000 -0.253 0.000 Calculated T Value Calculated T Value “ _ 2 0. 0. 876 0.000 0.000 409 1. “ --- ~ 1 --- 000 1 2 . . 0. 7530.493 1.056 1.067 436 1. -0.592 -0.781 ratio data and for percent heavy minerals in 120+230 2 4 1 0.000 1 0 33 0. 72 2 S 4 S LM LM V ar. Var. level Mean Mean . 818 . 3.133 3.1723.021 2.670 3 2.578 2 4.095 3.331 2.249 5.530 2.034 2.512 0.100 25 14 12 49 21 25 21 14 12 49 T T Test for sand/mud mesh mesh sands. Si ze Si Var. Var. Size Var. Var. ra tio data • • 1. 503 1. 1.657 382 1. 423 1. 4.095 1.051 2.249 1. 1. 758 27 1.608 27 Dev. Std. 2.480 Dev. Std. 4.042 * * significant at 11.890 Sand/mud TABLE 10 TABLE Percent heavy minerals in 120+230 mesh sands Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 128 * t-" O o o o o 0 3 O 03 1 1 1 1 CM O cn 0 3 O CC • • +-> o o CO O 03 1 T5 G ■K O o O O ‘H o o O 0 3 P s t 1 1 1 O CM I O 0 3 u p • • 03 o o o to P 1 • P o i E- X G3 P 0 o p o r " o o P o o o o 4 4 •H 1 1 r - 1 •H * -O * •3C •K •H O O oo LO o t o 00 CM P O CM Mt LO o LO H - O cu rH O LO LO P t 1 o 0> CM O 0 • • • • • • • • u o p o o o CM 1 1 C/3 3 c/) u P rH CM t o P J2 03 P •P G r j cO rH CM tO p - ^ 03 4-> > > r-J 0 r-c 5b CO £ X . r-1 LO LO LO 'O' CO tH • G t o 03 P PG t"- O 00 rH rH tO P G CM rH P •rH G 0 OO LO O P CM p G 0 00 r-» o tH > s • ••••• > 2 • P IS) O LO CM tO O 'O' Ex t/3 G •H H H tH tO tH G CO *H C M C M i—1 i—I 'O ’ CM 3 > 03 P 03 03 O Is* to CTi to O CO G3 > rH rH «a tso P 0 • ••••• P P 0 • • < G 3/3 =1 O t—It—1 H i—1 t—! 1 03 n o o ** ** significant at 0.050 level E- s X * significant at 0.005 level Reproduced with permission of the copyright owner. Further reproduction prohibited without permission. 129 - - s 0.000 11.610' - -- LM 0 .000 11.610* _ “ - - 4 0 .0 0 0 “ --- — 0 .0 0 0 -1.151 Calculated T Value “ 2 .101* 8 0 .0 0 0 “ --- 1 6.356* -0 . 562 . -0 12 0 .0 0 0 3 7.784* 9.918* S LM V ar. Var. Mean 0. 337 0. 0.161 0. 316 4 0. 350 0.170 49 0.166 27 21 14 12 Size Var. 0.073 25 0.051 0.072 0.772 0.045 0.059 Eld. Dev. * * significant at 0.005 level TABLE 12. TABLE T Test for garnet/epidote+hornblende data. Reproduced with permission of the copyright owner. Further reproduction prohibited without permission.